MR 82-15

Regional Geology of the Southern Lake Erie
(Ohio) Bottom: A Seismic Reflection and

Vibracore Study
‘ WHOI
y DOCUMENT
Charles H. Carter, S. Jeffress Williams, COLLECTION

Jonathan A. Fuller, and Edward P. Meisburger

MISCELLANEOUS REPORT NO. 82-15
DECEMBER 1982

Se
“Sezmine Be

Approved for public release;
distribution unlimited.

U.S. ARMY, CORPS OF ENGINEERS
COASTAL ENGINEERING
RESEARCH CENTER

Kingman Building
a Fort Belvoir, Va. 22060
ee
2.06
USB

Me &2-15

Reprint or republication of any of this material
shall give appropriate credit to the U.S. Army Coastal
Engineering Research Center.

Limited free distribution within the United States
of single copies of this publication has been made by
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Contents of this report are not to be used for
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Citation of trade names does not constitute an official
endorsement or approval of the use of such commercial
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The findings in this report are not to be construed
as an official Department of the Army position unless
so designated by other authorized documents.

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READ INSTRUCTIONS
REPORT DOCUMENTATION PAGE BEFORE COMPLETING FORM
T. REPORT NUMBER 2. GOVT ACCESSION NO, 3. RECIPIENT'S CATALOG NUMBER
MR 82-15

4. TITLE (and Subtitle) 5. TYPE OF REPORT & PERIOD COVERED

REGIONAL GEOLOGY OF THE SOUTHERN LAKE ERIE (OHIO)| 4, 0011 f
BOTTOM: A SEISMIC REFLECTION AND VIBRACORE OE aa eRe oA TOS Ce

STUDY 6. PERFORMING ORG. REPORT NUMBER

7. AUTHOR(s) 8. CONTRACT OR GRANT NUMBER(s)

Charles H. Carter, S. Jeffress Williams,
Jonathan A. Fuller, and Edward P. Meisburger

9. PERFORMING ORGANIZATION NAME AND ADDRESS 10. PROGRAM ELEMENT, PROJECT, TASK
AREA & WORK UNIT NUMBERS

Department of the Army
Coastal Engineering Research Center (CEREN-GE)
Kingman Building, Fort Belvoir, VA 22060

11. CONTROLLING OFFICE NAME AND ADDRESS 12, REPORT DATE
Department of the Army December 1982
Coastal Engineering Research Center 13. NUMBER OF PAGES

Kingman Building, Fort Belvoir, VA 22060 109
14. MONITORING AGENCY NAME & ADDRESS(if different from Controlling Office) | 15. SECURITY CLASS. (of thie report)

C31665

UNCLASSIFIED

1Sa. DECL ASSIFICATION/ DOWNGRADING
SCHEDULE

16. DISTRIBUTION STATEMENT (of this Report)

Approved for public release; distribution unlimited.

17. DISTRIBUTION STATEMENT (of the abstract entered in Block 20, if different from Report)

18. SUPPLEMENTARY NOTES

19. KEY WORDS (Continue on reverse sida if necessary and identify by block number)

Geomorphology Sand resources Seismic reflection
Lake Erie Sediments Vibracores
Ohio

20. ABSTRACT (Continue em reverse sides if neceasary and identify by block number)

The southern part of the Ohio waters of Lake Erie between Conneaut and
Marblehead was surveyed in August of 1977 and 1978 to acquire knowledge of the
nature, distribution, and geometry of the lake deposits. Primary data consist
of 576 kilometers of seismic reflection trackline profiles and 58 vibracores
ranging from 0.7 to 6.1 meters long. About 23 percent of Ohio's part of Lake
Erie was covered by the survey.

(Cont inued)

DD ont, 1473 Ecprmion oF t ov 651s OBSOLETE UNCLASSIFIED

SECURITY CLASSIFICATION OF THIS PAGE (When Data Entered)

UNCLASSIFIED
SECURITY CLASSIFICATION OF THIS PAGE(When Data Entered)

Devonian shale overlain by Quaternary glacial tills and postglacial
deposits underlies most of the survey area. In general, the shale is exposed
nearest the shore and is succeeded offshore by till and postglacial deposits.
The shale surface is commonly more irregular than the till and postglacial
deposit surfaces; slopes on the lakeward dipping shale surface range from
about 5 to 20 meters per kilometer.

Pleistocene tills--both basal and flow tills--also underlie most of the
survey area with extensive exposures between Fairport Harbor and Avon Lake
and off Lorain. Interlaminated silts and clays are interbedded with the
flow till in some cores; three cores contain both basal and flow tills. The
tills are made up largely of silt and clay-size particles composed of quartz
and illite. The till has a flatter and more uniform surface than that of the
underlying shale, with lakeward slopes ranging from about 1 to 4 meters per
kilometer. The till varies in thickness from 0 to 26 meters and thickens
lakeward at about 5 meters per kilometer.

Sand, muddy sand, sandy mud, and mud are the four principal postglacial
deposits. These deposits commonly lie lakeward and overlie rock and till.
In general, the coarser deposits lie nearest the shore. However, the two
principal sand deposits at Fairport Harbor and Lorain-Vermilion are well
offshore. Also, the finer deposits are found closer to shore and in shallower
water west of Cleveland. Combined postglacial deposit thicknesses range
from 0 to 22 meters and like the till, the postglacial sediment thickens
lakeward.

The tills were first deposited on an irregular, erosional shale surface.
Till deposition continued intermittently on both shale and previously
deposited till until eastward retreat of the last Wisconsinan glacier from
the Erie basin. Drainage of the lake ponded west of the glacier then exposed
the till to subaerial erosion which led to the formation of stream channels
in the till off Lorain and Fairport Harbor. Isostatic rebound of the outlet
then led to a rise in lake level with associated erosion and deposition along
the expanding lakeshore, which tended to smooth the till surface. The early
postglacial (Holocene) deposits, which accumulated during the rise in lake
level and cover the underlying till and shale, were deposited in a complex of
fluvial, deltaic, and lacustrine environments. Modern lacustrine muds are
now being deposited over these early Holocene deposits.

2 UNCLASSIFIED

SECURITY CLASSIFICATION OF THIS PAGE(When Data Entered)

PREFACE

This report is one of three reports which describe results of the Inner Continental Shelf Sediment
and Structure (ICONS) study of southern Lake Erie. The first report (Williams, et al., 1980) deals with
the sand resources in Ohio and the second report (Williams and Meisburger, 1982) provides survey results
from Pennsylvania. The primary objective of the ICONS program is to locate and delineate sand and
gravel deposits suitable for beach nourishment and restoration (Duane, 1968). The work was carried out
under .the U.S. Army Coastal Engineering Research Center's (CERC) Barrier Island Sedimentation Studies
work unit, Shore Protection and Restoration Program, Coastal Engineering Area of Civil Works Research
and Development, in cooperation with the Ohio Department of Natural Resources, Division of Geological
Survey (DGS).

The report was prepared by Charles H. Carter and Jonathan A. Fuller, Geologists, under the general
supervision of H.R. Collins, Chief, DGS, and by S. Jeffress Williams and Edward P. Meisburger, Geologists,
under the general supervision of Dr. C.H. Everts, Chief, Engineering Geology Branch, and Mr. N. Parker,
Chief, Engineering Development Division, CERC. Data collection was conducted by CERC and DGS with the
assistance of U.S. Army Engineer Districts, Buffalo and Mobile, and the U.S. Army Engineer Waterways
Experiment Station (WES).

The authors acknowledge the assistance of a large number of people who contributed to the success of
this study. J. May, J. Forbes, and D. Andrews of WES operated the seismic reflection equipment; E. Lagrone
of the Mobile District operated the vibracore equipment; and M. Chambers of the Buffalo District skippered
the tug and scow for the vibracore operaticn. Within DGS, D.L. Liebenthal skippered the boat carrying the
seismic reflection equipment and the navigation system; D.E. Guy, Jr., C.L. Hopfinger, T.J. Feldkamp,

J.D. Reed, and J. Vormelker positioned the transponders for the Mini Ranger; R.W. Carlton provided the
X-ray diffraction analyses; and C.L. Hopfinger helped throughout with the laboratory work on the vibra-
cores, with data compilation in the office, and with identification of the mollusks, with the aid of

M.J. Camp of the University of Toledo. N.A. Rukavina (Environment Canada) provided helpful comments on
parts of the report. In addition, G.P. Hall and J.C. Dixon of the Ohio Department of Transportation pro-
vided the Atterberg limits, and T.L. Lewis of Cleveland State University had the radiocarbon work done.
D.A. Prins of CERC served as field survey chief during both data collection phases, and D.J. Benson,
formerly of DGS, helped plan the field surveys and took part in the seismic reflection survey. Lastly,
C.H. Everts and H.R. Collins made constructive reviews and their comments are appreciated.

Original copies of all seismic data are stored at CERC. Cores collected during the field survey
program in Ohio are in a repository at the University of Toledo, under agreement with CERC. Requests
for information relative to these items should be directed to CERC or the Department of Geology,
University of Toledo.

Technical Director of CERC was Dr. Robert W. Whalin, P.E., upon publication of this report.

Comments on this publication are invited.

Approved for publication in accordance with Public Law 166, 79th Congress, approved 31 July 1945,
as supplemented by Public Law 172, 88th Congress, approved 7 November 1963.

Yh lan ’
TED E. BISHO

Colonel, Corps of Engineers
Commander and Director

Il

IIl

IV

APPENDIX
A

B

CONTENTS

CONVERSION FACTORS, U.S. CUSTOMARY TO

IENIENODIUGIEOIN, “GGG 66 6 6 0 OOO
1. Background and Scope ......
oe iwai@ilcl PO CCGMEOAS 6 oo 66) 66 6
3. Office and Laboratory Procedures .
4. Seismic Interpretation .....
Bo EEN ALOIS) SEWNCELAS) (5 5 o lo li5 6 6

IA EDLSILGNL, SIRLIIONS og yao on O00 0
IG Ieiereexralyetesteyn 1G Go) Bi9. 6 a lio oo 9
Ao SMOKES 6 6 6 0 690 '0 Golo Mono o
Se, WEST 6 60 boo 6 6 oye

HOMME O MIDI AOSIOUS “Solo lo 6 oo ag 6 6

Ibo

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re
4,

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Sate eerie ol eral reua sunesmuloneeeint sitcernionite
eDiets cuarcyehortra ctale ous minor camneil wm ouke Shanes

Postglacial Sediment ......

GMOLOGIG WOO. 56 6 Go oo 6 Oo

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SRW ig, -OMSo ca 01) 01 Como ake a0
nRaHI Ey Unga Hoke “opi ceiage Sor sous. WORuIG ko
Postglacial Sediment ......

SOMMMINIRE G5 0 oo Ol0 G6 6 6 “G0! Ic

UA IBOVAEWID, (CIA) Gg 1g 6. oO OO 40-0

CORE SEDIMENT DESCRIPTIONS .

GRANULOMETRIC DATA AND CUMULATIVE

X-RAY DIFFRACTION ANALYSES ... .

ATTERBERG LIMITS .

MOLLUSK IDENTIFICATIONS FROM CORES .

METRIC (SI)

CURVE PLOTS

e ° e °

SEDIMENT THICKNESS DATA FROM SEISMIC RECORDS

CALCULATIONS OF SEISMIC VELOCITY IN WATER...

CALCULATIONS OF SEISMIC VELOCITY IN POSTGLACIAL SEDIMENTS

COMPARISON OF POSTGLACIAL SEDIMENT THICKNESSES AS
MEASURED FROM THE CORES AND CALCULATED FROM THE
SEISMIC RECORDS ... .

. ° °

42

45

Us

92

94

5)

97

107

108

109

14

15

16

17

18

19

CONTENTS
TABLES
Surface-sediment echo character and their interpretation .
Properties of basal till and flow till in study area. .
FIGURES
Lake Erie study area, from Conneaut to Marblehead, Ohio

Trackline location map, Ohio-Pennyslvania State line to east of
Basliepore Geyer 55616 510 60 0 o 0 OO 6b Oo 6 8 Ob OO 8

Trackline location map, east of Fairport Harbor to Northeast
Wacine GUM 96 6.g co vowoua-o 00 6 60 08.0006 oro Sol dole

Trackline location map, Northeast Yacht Club to Avon Point .
Trackline location map, Avon Point to Vermilion ...
Trackline location map, Vermilion to Cedar Point ......
Trackline location map, Cedar Point to Long Beach

The DGS Research Vessel GS-1 used to tow the seismic equipment
Biol NOCHEG CORE SEES 6 0 5166 06 6 56 6 610 00.6 056.0 6 6

A 6-meter-long vibratory coring apparatus used to collect
SEG CORES 5 60 6 0 06 0 06 6 50

The U.S. Army Engineer District, Buffalo, tugboat Washington .
Seismic record showing character of shale reflector

Seismic record showing internal reflectors in till deposit. .

Rock structure contour map as interpreted mainly from the seismic

BEC ELON Ime CORG'S is wisy Wes ceh ton arian col ans cule USE eM rattan tae aneran tos Wo. ere

Till structure contour map as interpreted mainly from the seismic

Teerileciealeia imecorlss 66 5 00 6 6 6 016 6 610° 6 oO 0 O16
MOE), OF, DgiSeul waliLily sin. Corea 7/2) eles sowie Wom Gea 6 Wel i6s 86 oe c
HINOEO OE sEdlory tesll si Core 98 oo 5 6 66 0 56 00 oo
Photo of varved (?) clay in core 98 .....

Seismic record showing the smooth surface echo character of the
clloyy teslll sim Eine Cileyellemal ae 6 6 6 6 6 ob oo

Seismic record showing the irregular surface echo character of
BlovS BoM ugg Go Bole of obo) & ay eco 6

Page

10

11

12
13
14
15

16

17

18
19
22

23

By

28
29
29

BY)

Sal

32

20

“al,

22

23

24

25

26

CONTENTS
FIGURES—-Continued

Till isopach map as interpreted mainly from seismic reflection
aAeEOIS. 6 S600 0 6 loli6 600 00 6 0 66 606 0 6,0 6 0.00

Map of surface sediments as interpreted from the seismic
reflection records and core samples . .......+.-. «© « « »

Welee) Che Sekavel abn Core YS 56 O06 6 65.666 0.5 66060006 0 6
Invoeloy Cpe rsinrekaby, eral hn Coie VAG og oso 6 O 6 6 0.0000 6 6
IWovoyere) Cpe. epee pmol ish Copa GY) oi'6 5 O10 010 0 (06 016 6016.0 0 6
aver) Ghz wntyel) stl COVES IS 1G Goo o Galo 'o oo G6 oo 66.006

Postglacial sediment isopach as interpreted mainly from seismic
sqnEilererealoyn <Teeorals: |G 56 6 6 6 6 006 09 010 600 0 0/0 0 0 0

Page
34

35
36
36
37

37

38

CONVERSION FACTORS, U.S. CUSTOMARY TO METRIC (SI) UNITS OF MEASUREMENT

U.S. customary units of measurement used in this report can be converted to
metric (SI) units as follows:

Multiply by To obtain

inches es ; millimeters
2.54 centimeters
Square inches 6-452 Square centimeters
cubic inches 16.39 cubic centimeters
feet 30.48 centimeters
0.3048 meters
square feet 0.0929 Square meters
cubic feet 0.0283 cubic meters
yards 0.9144 meters
Square yards 0.836 Square meters
cubic yards 0.7646 cubic meters
miles 1.6093 kilometers
Square miles 259.0 hectares
knots 1.852 kilometers per hour
acres 0.4047 hectares
foot—pounds 1.3558 newton meters
miniciere Lai" se 1072 kilograms per square centimeter
ounces 28.35 grams
pounds 453.6 grams
0.4536 kilograms
ton, long 1.0160 metric tons
ton, short 0.9072 metric tons
degrees (angle) 0.01745 radians
Fahrenheit degrees 5/9 Celsius degrees or Kelvins!

1T obtain Celsius (C) temperature readings from Fahrenheit (F) readings,
use formula: C = (5/9) (F -32).
To obtain Kelvin (K) readings, use formula: K = (5/9) (F -32) + 273.15.

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MEU ity ase Ov 7

REGIONAL GEOLOGY OF THE SOUTHERN LAKE ERIE (OHIO) BOTTOM:
A SEISMIC REFLECTION AND VIBRACORE STUDY

by

Charles H. Carter, S. Jeffress Willtams,
Jonathan A. Fuller, and Edward P. Metsburger

I. INTRODUCTION

1. Background and Scope.

The construction, improvement, and periodic maintenance of beaches and
dunes by the placement (nourishment) of suitable sand along the shoreline is
an important means of counteracting coastal erosion and enhancing recreational
facilities. However, it has become increasingly difficult in recent years to
obtain suitable sand from traditional sources such as lagoons and inland
deposits because of economic and ecological factors. This problem led the
U.S. Army Coastal Engineering Research Center (CERC) to initiate a search for
offshore sand deposits. Exploratory efforts to locate and inventory deposits
suitable for future fill requirements began in 1964 with a survey off the New
Jersey coast (Duane, 1969). Subsequent data collection surveys have included
the Inner Continental Shelf areas off New England, Long Island, Delaware,
Maryland, Virginia, Florida, the Cape Fear region of North Carolina, eastern
Lake Michigan, and southern California. This program, formerly known as the
Sand Inventory Program, is now known as the Inner Continental Shelf Sediment
and Structure (ICONS) program.

The type of data collected for the ICONS program is not only useful in
locating potential borrow areas but is of further value in providing geological
information for planning, design, and environmental impact evaluation of coastal
engineering works. The results of the ICONS studies are normally presented in
two separate but complementary reports: one covering sand resources, the other
covering the regional geology.

This study is unique from the previous ICONS studies in that it was con-
ducted in cooperation with a State geological survey, the Ohio Department of
Natural Resources, Division of Geological Survey (DGS). The report deals
primarily with the bottom and subbottom deposits in the Ohio waters of Lake
Erie as mapped largely from high-frequency seismic reflection profiles and
vibracores between Conneaut (at the Ohio-Pennsylvania border) and Marblehead.
The report does not include the reach between Marblehead and Toledo. Seismic
profiling of this reach was done, but no vibracores were taken and the seismic
records are difficult to interpret because of the lack of well-defined reflec-
tors. The lack of well-defined reflectors on the records between Vermilion and
Marblehead also precluded mapping of the subbottom deposits along this stretch
of shore. This report follows a report on sand resources in Ohio (Williams,
et al., 1980) and another report on the Pennsylvania part of Lake Erie
(Williams and Meisburger, 1982).

The study area encompasses a zone ranging from 1 to 16 kilometers offshore
between Conneaut and Marblehead (Fig. 1). Survey coverage of the area is shown

. g3° i ae 81° 80° 79°
43

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ONTARIO ee
MICHIGAN | p
Long Pt. .~
——— e
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a: ~ Ey states
j ene NEW YORK
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SS D STUDY AREA Conneaut
eS eZ <
Mi: OS Fairport mectee PENNSYLVANIA
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Sandusky &
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H 100 Kilometers
OHIO | 0 20 40 60 8010

41° 41°
oe
83° 82° a1? 80° 79

Figure 1. Lake Erie study area, from Conneaut to Marblehead, Ohio.

in Figures 2 to 7. Data collected for this study consist of 576 kilometers of
seismic reflection trackline profiles, taken in August 1977, and 58 vibracores
ranging from 0.7 to 6.1 meters long, taken in August 1978. About 23 percent
of Ohio's open lake part of Lake Erie (7481 square kilometers) was covered by
the seismic reflection survey between Conneaut and Marblehead.

The survey data in this report were supplemented in places by previous DGS
work. Vertical control was obtained from National Ocean Survey (NOS) water
level gage data for Lake Erie; water depths are referenced to low water datum
(LWD), which is 173.3 meters above mean water level at Father Point, Quebec
(International Great Lakes Datum (IGLD), 1955). Mean lake level in both
August 1977 and August 1978 was about 1 meter above LWD. This study is basi-
cally reconnaissance in nature, as seismic line spacing and orientation and
core spacing density preclude a detailed evaluation of the bottom and subbottom
deposits. However, because of the relatively flat-lying nature of the deposits,
extrapolation between tracklines can be made with a fair degree of confidence.

2. Field Procedures.

a. Geographic Positioning System. A radar-type electronic positioning

system, the Motorola Mini-Ranger III, was used to determine position of the
research survey vessel during the seismic survey (phase I) and the vibracoring
(phase Il). The system determines the position of the survey vessel with
respect to two known reference points on shore and is restricted to line-of-
sight operation. The basic system consists of a master mobile unit mounted
onboard the vessel and two shore-based transponders. The master unit triggers
reply pulses from the transponders; each transponder pulse is received sepa-
rately and the elapsed time between the transmitted pulse and the individual
transponder reply pulse is converted to a measurement of distance. Each
distance (range) from the two transponders at the known shore stations is dis-
played in turn on the range console. This range information, together with
the known locations of the shore stations, is then trilaterated and plotted

on hydrographic charts to obtain the position (fix) of the survey vessel.

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Navigational fixes during the seismic survey were obtained about every 2 minutes
and each fix was keyed to the seismic records by an event mark on the records.

b. Seismic Reflection Profiling. Seismic reflection profiling is widely
used to delineate geologic features on land and over water. In this study,
repetitive high-energy sound pulses were generated near the water surface to
produce seismic waves, which reflected off the geologic features; these waves
were received and recorded on paper by a recorder aboard the survey vessel to
produce a cross section representing the features at and below the lake bottom.

The seismic reflection data were obtained by towing the sound-generating
and receiving instruments behind the DGS research vessel, GS-1 (Fig. 8), which
followed predetermined survey tracklines (Figs. 2 to 7). In phase I of this
study, two seismic subbottom profiling systems were used simultaneously: an
Ocean Research Equipment, Inc. (ORE) 3.5-kilohertz pinger system and an Edgerton,
Gremerhausen and Greer (EG&G), Inc. UNIBOOM system. The pinger records were of
little use because of their lack of resolvable reflectors, whereas the UNIBOOM
records were generally good. The inshore boundary of the survey was about 1
kilometer from shore and the offshore boundary was about 7 kilometers offshore.
The nearshore survey water depths were about 7.5 meters, which is about the
minimum depth for obtaining good-quality seismic profiles; the offshore water
depths were about 14 meters. Information on various seismic profiling tech-
‘niques is discussed in Ewing (1963), Moore and Palmer (1967), Barnes, et al.
(1972), and American Association of Petroleum Geologists (1977).

Figure 8. The DGS Research Vessel GS-1 used to tow the seismic
equipment and locate core sites.

17

c. Coring Equipment. A pneumatic vibratory coring device designed to
obtain continuous sediment cores a maximum of 6.1 meters long was used in the
phase II survey operation (Fig. 9). The apparatus is equally effective in
penetrating and recovering granular and cohesive sediments; however, a stony
till is not easily penetrated and the core barrel will not penetrate coherent
rock. The core rig consists of a 10-centimeter steel core barrel, clear plas-
tic inner liner, shoe and core catcher, and a pneumatic driving head attached
to the upper end of the barrel. These elements are enclosed in a quadrapod-
like frame with four articulated legs which rest on the lake bottom. An
aluminum H-beam and frame serve as a support structure and guide for the vibra-
tor head and core pipe as the core barrel penetrates the lake bottom. The lack
of rigid attachment of the coring device to the surface vessel allowed limited
motion of the vessel during the actual coring processes. Power was supplied to
the pneumatic vibrator head by a flexible hoseline connected to a large-capacity
(118 liters per second) air compressor. After coring was completed, the assem-
bly was hoisted onboard the vessel, the liner containing the core was removed,
samples from the top and bottom of the core recovered, the ends sealed, and the
core carefully marked for orientation and identification. The historical
development of vibratory coring equipment is discussed by Tirey (1972).

Figure 9. A 6-meter-long vibratory coring apparatus used to
collect sediment cores is shown being lifted off
the platform for deployment on the lake floor.

A 36-meter-long scow from the U.S. Army Engineer District, Buffalo, was
used as the platform for phase II coring. The scow was transported by the
Corps tugboat Washington (Fig. 10).

18

Figure 10. The U.S. Army Engineer District, Buffalo,
tugboat Washtngton.

d. Data Collection. Before the fieldwork began, seismic survey tracklines
were plotted on navigation charts of the survey area. Position, spacing, and
length of the tracklines were determined by several factors. The primary
concern was spacing the lines to achieve maximum coverage of the study area
within the limits of time and budget. After the survey tracklines were selected,
the locations of the shore stations for the navigation system were determined.
Of high priority were stations at elevated positions (for adequate line-of-
sight), which also offered good triangular position in relation to the survey
vessel and adjacent shore stations. (Acceptable results are achieved when the
angle of range intercept of the vessel is greater than 30° and less than 150°;
optimum range angle intercept is 90°.) A total of 32 shore navigation stations
were used along 207 kilometers of coast from Conneaut to Marblehead. Positions
and spacing of the tracklines were altered at times to gather additional infor-
mation on geologic features such as buried stream channels, sediment contacts,
and probable lake bottom exposures of sand.

Interpretations of the seismic profile records were made to select coring
sites with the greatest potential for sand and subsurface information. These
records were visually examined and marked to establish the primary geologic
features (e.g., regional sedimentary reflectors, sediment contacts, buried
stream channels). Selected acoustic reflectors were then mapped to provide
areal continuity of horizons considered significant because of their areal
extent and relationship to the general structure and geology of the study area.
The use of seismic data’ to interpret geologic conditions before selecting the
core sites maximizes the usefulness of both sources of data and provides the
most efficient use of funds.

19

During phase II, the vessel GS-1 was used to relocate fix positions
selected as coring sites by duplicating the range values from the shore sta-
tions. The GS-1 first maneuvered until one of the ranges was duplicated and
then an arc was run on that range until the other range was intersected, at
which time an anchored float was used to mark the core location. Core sites
were located and marked in this manner because of the limited maneuverability
of the scow. The GS-1 crew located a core position in minutes and dropped a
float marker; the tug and scow then moved in on the marker, anchored, and the
core rig was lifted from the deck of the scow and set on the lake bottom.
Meanwhile, the GS-1 proceeded to the next core site. Once the core rig was on
the bottom, the core barrel was driven into the lake bottom sediments; within
about 15 minutes the coring was completed and the apparatus was lifted back
onto the scow. The core liner containing the sediment was removed from the
barrel and small reference samples were obtained from the top and the bottom of
each core. The liner was then capped and sealed, labeled, and a general de-
scription of the samples was made. The scow was then moved to the next coring
location. While underway, the corer was reassembled and loaded with a new
liner. In general, the corer penetrated the lake bottom deposits quite easily;
however, penetration in stony till and in some well-sorted, medium-grained
sands was poor.

3. Office and Laboratory Procedures.

After completion of the data collection, the navigational fix marks, ship
trackline positions, core sites, and shore stations were plotted to show the
coverage in the survey area (Figs. 2 to 7). The cores were split longitudinally,
using a circular powersaw to cut the plastic liner and a piece of thin wire to
cut the sediment. As soon as the core was opened it was color typed using the
Munsell color system (Munsell Soil Color Charts, 1954 ed., Munsell Color, Inc.,
Baltimore, Md.). Color typing was immediately followed by sampling for
natural water determinations (sample is weighed, dried, and reweighed), by
unconfined compressive and shear-strength measurements (using hand-held Soiltest
instruments), and by detailed descriptions (see App. A). The unsampled half of
the core was wrapped in plastic for storage. After the sampled half had par-
tially dried (a day or two), the description was checked, photos of representa-
tive units were taken, and additional sampling was done if necessary.

Three principal techniques were used for the grain-size analyses: rapid
sand analysis (RSA) for the finer sands (U.S. Army, Corps of Engineers, Coastal
Engineering Research Center, 1977), sieve analysis at 0.5-phi intervals for the
coarser sands and fine gravel (Folk, 1974), and pipet analysis for the samples
containing appreciable clay- and silt-size particles (Folk, 1974) (App. B).

In addition, 22 clay samples were analyzed by X-ray diffraction (App. C), and
general sand-grain mineralogy was determined with a binocular microscope using
a feldspar stain technique (Gross and Moran, 1970). Atterberg limits were
determined for 29 fine-grained samples (App. D), and two radiocarbon-14 ages
were determined from wood samples in core 62. Mollusks from selected samples
were identified generally to species level (App. E).

4, Seismic Interpretation.

Seismic reflections from the shale and till surfaces were extensive enough
in the subbottom to be mapped throughout most of the study area. The shale
reflector generally is broken and irregular but well defined with closely

20

spaced internal reflectors which either intersect the main reflector at a low
angle or parallel it in a regular pattern (Fig. 11). On the other hand, the
till reflector generally is continuous and not as irregular nor as well defined
as the shale reflector. Im addition, irregular but fairly continuous internal
reflectors are fairly common in the till (Fig. 12). The shale and till reflec-
tors were mapped at two confidence levels. The first confidence level was used
where the reflector was well defined on the seismic record. The second confi-
dence level was used where the reflector was not as well defined but its
position could be reasonably well inferred from the overall geologic setting
and character of the reflector. In addition, the echo character type of the
surface sediment, in conjunction with reference sediment samples, was used to
map the surface sediment. Seven surface echo character types were defined:
rock, till, sand, muddy sand, sandy mud, mud, and rock waste (Table 1).

Following the mapping of the reflectors, acoustic traveltimes were meas-
ured to determine sediment thicknesses (App. F). The velocities of sound
through the till and postglacial sediment are used to convert these measure-
ments into sediment thickness. The velocity of sound in water was calculated
to be about 1.54 kilometers per second from measured depths at several core
locations (App. G). The average velocity in the postglacial sediment was calcu-
lated to be about 1.3 kilometers per second in a similar way by using the thick-
ness of the postglacial sediment in the vibracores (Apps. H and I). A velocity
for the till was not calculated because none of the cores penetrated till to
rock; however, laboratory work by Morgan (1964) suggests that 1.8 kilometers
per second is a realistic velocity for Lake Erie till so this value was used
in the calculations.

5. Previous Studies.

The first comprehensive bottom sediment study of the Ohio part of the
central Lake Erie basin was done by Hartley (1961). Bottom grab samples were
taken on 1.6- or 3.2-kilometer grids and some subbottom sampling was done by
coring or jetting. Hartley's work provided important data that were used
extensively in the planning stages of this study. Shore and nearshore deposits
within 610 meters of the shoreline were mapped in the 1970's as part of DGS's
county shore erosion studies (Benson, 1978; Carter and Guy, 1980); this infor-
mation was used in the current study to map the sediment adjacent to the shore.
Also, several hundred kilometers of seismic reflection profiles and 32 borings
and vibracores were collected in a rectangular nearshore area off Cleveland
(Dames and Moore, 1974).

Three shallow seismic reflection surveys of central Lake Erie have been
reported (Morgan, 1964; Lewis, 1966; Wall, 1968). The works by Morgan (1964)
and Wall (1968) are too general to be of use, whereas the work by Lewis (1966)
is sufficiently detailed, particularly on the geologic history of the lake,
and of use.

II. PHYSICAL SETTING
1. Introduction.

The Lake Erie basin is underlain by middle Paleozoic sedimentary rocks that
are overlain by Pleistocene- and Holocene-age deposits. The Pleistocene deposits

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Table 1.

Surface-sediment echo character and their interpretation.

Echo character Sediment interpretation Letter
designation

Very poor multiple, | smooth surface,
mostly transparent, may have conti-
nuous, multiple, parallel internal
reflectors.

Very poor to poor multiples, !
slightly irregular surface (rougher
than M), nontransparent (a noisy
record).

Good multiples! (commonly two to
three), smooth to slightly
irregular surface (similar to X),
nontransparent.

Fair multiples, ! hummocky to gently
rolling but smooth surface,
commonly nontransparent.

smooth or irregular surface (in
between S and R), commonly irregu-
lar internal reflectors.

Fair to good multiples (commonly
three or more), commonly a broken,
irregular surface (may look similar
to T), and may have closely spaced
discontinuous, internal reflectors.

Fair to good multiples and a
jagged, irregular surface.

Poor to good multiples (mostly fair),

Soft, nearly fluid mud

Sandy mud

Muddy sand

Clay and clay with gravel
(probably till)

Rock (probably shale)

Rock waste (shale derived
from a harbor excavation)

lVery poor multiple:

Poor multiples:
discontinuous.

Fair multiples:
continuous.

Good multiples:
are commonly continuous.

a discontinuous multiple if present.

24

RW

one to two multiples; the first multiple is commonly

one to two multiples; the first multiple is commonly

two to seven multiples; the first and second multiples

consist largely of glacial till and the Holocene deposits consist largely of
fine-grained lake sediments. About 14,000 years before present (B.P.) a glacial
lake occupied the Lake Erie basin to an elevation of about 244 meters above sea
level (Sly, 1976). Within the next 1,400 years or so, lake level fluctuations
of a few tens of meters took place as the receding glacier, in a series of
retreats and advances, alternately exposed and buried different lake outlets.
The glacial activity ended about 12,600 years B.P. with retreat of the last
Wisconsinan glacier. This allowed the lake waters to discharge northeastward
across the Niagara escarpment, which at that time was depressed due to the
weight of the glacier. Because this outlet was about 40 meters below present
lake level, the level of early Lake Erie was at about 134 meters above sea
level. Subsequent isostatic rebound of the escarpment at the outlet led to the
filling of the lake to its present elevation of about 174 meters above sea
level.

2. Shore.

The shore from Conneaut to Huron consists of moderate to high relief (3 to
20 meters) shale and till slopes and bluffs commonly capped by old lake deposits.
The shale is exposed for appreciable lengths above or near lake level from
Conneaut to Fairport Harbor, near Euclid (Moss Point), between Cleveland and
Avon Point, and near Vermilion. The shore from Huron to Marblehead consists of
low relief (<2 meters) barrier beaches and laminated clay banks. The shore at
Marblehead consists largely of moderate relief (3 to 6 meters) dolostone and
limestone banks.

Beaches make up a fragmented band that front about 50 percent of the shore
in the study area. The beaches are commonly narrow (<15 meters wide) and
consist primarily of sand, although there are pocket beaches of cobbles in
places where the shore is composed of rock. In addition, there are about 3,000
shore protection structures consisting largely of groins and seawalls scattered
along the shore.

3. Offshore.

Lake Erie is the shallowest of the five Great Lakes with an average depth
of about 19 meters and a maximum depth of 65 meters. The nearshore slopes are
generally less than 1°; in the study area within 1 to 2 kilometers of the shore
the slope is about 0.25°, except between Fairport Harbor and Avon Point, where
the slope is about 0.50°. Offshore the slopes become gentler with a slight
decrease in slope from east to west; the area off Lorain-Vermilion is the prin-
cipal exception. In this area the offshore bottom rises to form a subtle ridge
(Pelee-Lorain ridge) which extends across the lake to Point Pelee, Canada.

Sand and gravel, generally less than 2 meters thick, cover much of the near-
shore (<1 kilometer offshore) bottom; most of the bottom farther offshore is
made up of fine-grained postglacial sediment, rock, till, or glaciolacustrine
clay (Verber, 1957; Hartley, 1961; Williams, et al., 1980). In general, the
distribution of these offshore deposits (to the international boundary) can be
divided into two areas: from Conneaut to Fairport Harbor, a band of shale is
bordered offshore by sand and finer postglacial sediment; from Fairport Harbor
to Marblehead, a band of sand and gravel, till, or rock (mostly shale) is
bordered offshore by finer, postglacial sediment except for till in the
Cleveland area and sand and gravel in the Lorain-Vermilion area.

25

IIL. BOTTOM DEPOSITS
1. Introduction.

Shale, till, and postglacial sediment ranging from sand to mud make up most
of the bottom deposits. Shale underlies most of the Ohio part of Lake Erie.
The shale is overlain by glacial tills that are overlain by postglacial deposits.
In general, the shale is exposed nearest the shore and succeeded offshore by the
tills and postglacial deposits.

2. Shale.

The contact between the Devonian limestones and dolomites to the west and
the Devonian shales to the east lies between Huron and Sandusky (Bownocker,
1920). The northeast trend of this contact, a gentle southeast dip, and shore
and nearshore exposures indicate that the Devonian Ohio Shale underlies most of
the survey area. In northern Ohio, the shale is made up of two carbonaceous,
blue-black shale members separated by a largely noncarbonaceous, blue-gray,
silty shale member (Hoover, 1960).

Shale is exposed close to the shore in a continuous 2-kilometer-—wide band
between Conneaut and Fairport Harbor, in a broken 1- to 2-kilometer-wide band
between Cleveland and Lorain, and in a continuous 2- to 3-kilometer-wide band
off Vermilion. The echo character of the shale surface on the seismic records
ranges from smooth to irregular (Fig. 11). In the subsurface, the shale reflec-
tor could be mapped along most of the tracklines; however, the reflector was
not apparent in places off Ashtabula, Fairport Harbor, Cleveland, and west of
Vermilion (Fig. 13).

The shale surface slopes lakeward between Conneaut and Ashtabula at about
10 meters per kilometer. West of Ashtabula, the slope is about 5 meters per
kilometer, decreasing to about 2 to 3 meters per kilometer at Fairport Harbor
and then increasing to about 10 meters per kilometer at Moss Point. The seismic
records do not show a shale reflector between Moss Point and west Cleveland.
From west Cleveland to Avon Point the slope is 15 to 20 meters per kilometer;
from Avon Point to west Vermilion the slope is gentler, about 4 to 6 meters per
kilometer. The irregular nearshore shale surface characterized by these
variable slopes is further exemplified by a major buried river valley (about
90 meters deep) entering Lake Erie at Cleveland (Crowell, 1979). In addition,
there are major valleys eroded into the shale at Huron (Stein, 1962) and
Lorain (Pree, 1962).

So Abatilale

Till overlies the Devonian Ohio Shale over most of the region covered by
the tracklines (Fig. 14). It can generally be characterized as a hard, stony,
unstratified deposit interpreted as basal till (Fig. 15; gravelly clay in
App. A) or a soft, clay-rich, commonly stratified deposit interpreted as flow
till (Fig. 16). Some of the till sections (e.g., cores 95, 98, and 100) con-
tain interlaminated silts and clays resembling varves (Fig. 17; clay in App. A);
cores 92, 98, and 99 contain both basal and flow till. The tills are made up
largely of silt- and clay-size particles composed of quartz and illite.

Detailed information on the texture, composition, and engineering properties
of the till is in Appendixes B and C; Table 2 is a summary of the information.

26

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Table 2. Properties of basal till and flow till in study area.

Color Olive gray Yellowish gray Olive gray Variegated

Grain size
(weight pct)
sand
silt
clay

Natural
(weight pct)

water content

Unconfined
compressive
strength (kg/cm?)

Shear strength
(kg/cm?)

Atterberg limits
liquid limit
plasticity index

INo data.

Two types of basal till were found in the cores. An olive-gray basal till
was found between Ashtabula and Fairport Harbor (cores 54, 55, 60, 61, and 70)
and between Avon Point and Huron (cores 77 to 80, 82, 86, 98, and 99); a
yellowish-gray basal till was found in the Lorain-Vermilion area (cores 84, 85,
92, 97, and 98). The yellowish-gray basal till overlies the olive-gray basal
till in core 98.

Flow till is found in the Cleveland area and between Lorain and Huron (cores
71 to 76, 81, 82, 92, 95, 96, 98, 99, and 100). A nearly structureless olive-
gray flow till with minor pea gravel and reddish-brown clay pods was found in
the Cleveland area (cores 71 to 76). The flow till between Lorain and Vermilion
(cores 81, 92, 95, 96, 98, 99, and 100) has contorted flow banding and ranges in
color from olive gray to dark yellowish brown. This flow till overlies a basal
till in cores 92, 98, and 99.

The basal till and flow till are exposed nearly continuously between
Fairport Harbor and Avon Point and between Lorain and Vermilion. Their surface
echo character on the seismic records ranges from smooth to irregular. In
general, the till in the Cleveland area has a smooth surface echo character
(Fig. 18); the till exposed both east and west has a more irregular surface
echo character (Fig. 19).

The till surface from Conneaut to Fairport Harbor slopes lakeward at 2 to
4 meters per kilometer. Between Fairport Harbor and west Cleveland the slope
is gentler, 1 to 2 meters per kilometer. From west Cleveland to Avon Point
the slope is steeper but fairly uniform at 2 to 3 meters per kilometer.

30

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Off Lorain-Vermilion the surface slopes lakeward toward the Pelee-Lorain
ridge at about 2 meters per kilometer to a depth of 23 meters before rising at
the same slope. In general, the till surface is fairly flat in contrast to the
underlying shale; however, topographic lows on the till surface were mapped off
Lorain-Vermilion (Hartley, 1960) and off Fairport Harbor (Wall, 1968).

The till thickens offshore, forming a wedge on the underlying rock; till
thicknesses determined from the seismic records range from 0 to 26 meters.
However, data indicate a till thickness of more than 28 meters off Cleveland
(Dames and Moore, 1974). Between Conneaut and Moss Point the till thickens
offshore at about 4 meters per kilometer. The till at west Cleveland thickens
offshore at about 31 meters per kilometer and then decreases uniformly west-
ward to about 6 meters per kilometer at Lorain (Fig. 20).

4. Postglacial Sediment.

Postglacial sediments ranging from sand to mud commonly lie lakeward of and
overlie rock and till (Fig. 21). The principal exceptions are off Cleveland,
where postglacial sediment is succeeded offshore by till, and west of Huron,
where postglacial sediment lies adjacent to the shore. The sediments can be
classified into four echo character types: sand, muddy sand, sandy mud, and
mud (Table 1; Figs. 22 to 25). In addition, rock waste from harbor dredging
was mapped off Ashtabula. In general, the sand is less than 0.5 millimeter in
diameter and is composed largely of subangular to subrounded grains of quartz,
feldspar, and rock fragments. The clay-size particles are similar in mineral-
ogy to the clays in the tili--mostly quartz, illite, and chlorite--although
several samples contain montmorillonite. Macrofossils (clams and snails) were
common in some cores, primarily in the coarser sediment. Specific data on the
texture, composition, engineering characteristics, and fossils of these deposits
are given in Appendixes B to E.

Between Conneaut and Fairport Harbor, muddy sand directly overlying shale
is generally found close to shore. This sediment is succeeded offshore by sandy
mud, which is commonly succeeded by mud. Between Fairport Harbor and Cleveland,
with the exception of the complex Fairport Harbor area, sandy mud was the only
postglacial sediment mapped at the lakeward ends of the traverses. Between
Cleveland and Vermilion mud generally lies lakeward of till or rock, although
coarser grained deposits lie offshore of the mud in the Lorain-Vermilion area.
West of Vermilion muddy sand is commonly succeeded lakeward by sandy mud. Sand
was mapped in three areas: Conneaut, Fairport Harbor, and Lorain-Vermilion;
see Williams, et al. (1980) for a discussion of the sand deposits at Fairport
Harbor and Lorain-Vermilion. Also, the finer sediments (mud and sandy mud) are
generally found closer to shore and in shallower water west of Cleveland.

The postglacial sediment increases in thickness offshore, except off Lorain,
reaching 18 meters between Conneaut and Fairport Harbor, nearly zero between
Fairport Harbor and Lorain, and up to 8 meters thick between Lorain and
Vermilion (Fig. 26). The thicknesses, however, are difficult to compare
because of the short (<5 kilometers) seismic traverses west of Cleveland.

Along the Conneaut to Cleveland reach, there is a principal difference at
about 9 kilometers offshore; from Conneaut to Fairport Harbor postglacial sedi-
ment thicknesses range from 10 to 16 meters, whereas from Fairport Harbor to
Cleveland there is an apparent lack of postglacial sediment. Along the

33

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Cleveland to Vermilion reach, with the exception of the area offshore of Lorain,
there is also a basic difference at about 5 kilometers offshore; from Cleveland
to Lorain postglacial sediment thicknesses range from 0 to 2 meters, whereas
from Lorain to Vermilion postglacial sediment thicknesses range from 4 to 5
meters. Offshore of Lorain, the postglacial sediment thickens to 8 meters
about 8 kilometers offshore and then decreases to the north as it pinches out
against the Pelee-Lorain ridge. Thus it appears that the nature and thickness
of the postglacial sediment is largely controlled by the configuration of the
underlying rock and till surfaces as well as by the existing wave climate.

IV. GEOLOGIC HISTORY
1. Introduction.

Sedimentary deposits from the Devonian and the Quatermary periods are
exposed in the study area. The Devonian Ohio Shale underlies most of the area
except for lower Devonian carbonates near Sandusky; Quaternary glacial and
interglacial Pleistocene deposits and postglacial Holocene deposits overlie the
Devonian rocks. A good general overview of the Quaternary geologic history of
the Lake Erie basin is given in Sly and Lewis (1972).

Bo Sines

Seismic reflection profiles extending the width of the central Lake Erie
basin illustrate the relatively irregular rock surface on a regional scale
(see Fig. 23 in Lewis, 1966). The irregular rock surface, as well as the
buried ancestral valleys of the Cuyahoga, Black, and Huron Rivers, indicates
that appreciable erosion of the shale has occurred. The relative narrowness
and northerly trend of these valleys, in addition to their Pleistocene fill,
imply that much of the erosion took place before Pleistocene Glaciation,
probably by streams.

So) aalalike

The relatively smooth till surface on the seismic records is judged to be
the product of several Wisconsinan glacial advances and retreats with glacial
and periglacial processes tending to smooth and fill irregularities in the
earlier glacial deposits. This hypothesis is consistent with the physical
variations in the deposits mapped from the seismic reflection records and the
internal reflectors, which indicate that the till is likely made up of multiple
till deposits. Field studies on both sides of the lake have documented multiple
Wisconsinan tills (Dreimanis, 1970; White and Totten, 1979). Following the
classifications of White and Totten (1979) and White (1979), the olive-gray
basal till in the cores is interpreted to be the Titusville-Millbrook Till and
the yellowish-gray basal till to be either the Lavery-Hayesville Till or the
Hiram Till.

The topographic lows in the till mapped off Fairport Harbor (Wall, 1968)
and Lorain-Vermilion (Hartley, 1960) are the most prominent features in the
till surface. In agreement with Wall's interpretation (1968), the lows repre-
sent channels cut into the till surface by eastward-flowing streams probably
following the retreat of the Erie glacier from the eastern end of the lake.

39

Lewis (1966) mapped two cross-lake moraines: The Erieau-Cleveland moraine
and the Pelee-Lorain moraine. The Erieau-Cleveland moraine extends from
Erieau, Ontario, to east of Cleveland, Ohio. The survey for the current study
did not extend far enough offshore to encounter this feature, but the trend of
the feature toward the U.S. shore (Fig. 21 in Lewis, 1966) indicates that the
feature might be related to the broad till platform mapped west of Fairport
Harbor. No evidence has been found of an end moraine along the Ohio shore that
would tie into this feature. Perhaps the moraine was eroded by streams follow-
ing glacial retreat or by waves and currents during the early lake stages.

The Pelee-Lorain moraine extends from Pelee Point, Ontario, to Lorain-
Vermilion, Ohio. The southern part of this feature was mapped in the survey;
however, as with the Erieau-Cleveland moraine, no evidence has been found of an
end moraine along the Ohio shore. As an alternate hypothesis perhaps the above
named tills were deposited by a glacier limited in extent to the present lake
boundaries and thus are younger than the hypothesized tills.

The overall scarcity of glaciolacustrine clay may be the result of Holocene
erosion. Erosion of the clay probably took place both subaerially and sub-
aqueously following retreat of the last Wisconsinan glacier from the Lake Erie
basin. This hypothesis is supported by modern erosion rates, which indicate
appreciably higher erosion rates of glaciolacustrine clay than of till (Carter,
1976). Coarse lag deposits overlying till, particularly in the Fairport Harbor
area, and beach deposits on the moraine off Erie, Pennsylvania (Williams and
Meisburger, 1982), appear to be good evidence for wave erosion during times of
lower lake levels. Lewis (1966) found coarse deposits overlying a smooth till
and glaciolacustrine clay surface along the north shore of Lake Erie; he inter-
preted the surface as a wave-cut terrace. This surface may be correlative with
the broad till surface between Fairport Harbor and Cleveland.

4. Postglacial Sediment.

Holocene sedimentation has contributed to a general filling in and flatten-
ing of the lake bottom. The sand deposits at Fairport Harbor, Lorain-Vermilion,
and Cedar Point (Williams, et al., 1980) are likely the product of different
depositional environments and different ages ranging from the early Holocene,
when lake levels were lower than at present, to the late Holocene. Two radio-
carbon ages were obtained from wood fragments in core 62 at Fairport Harbor
(T.L. Lewis, Cleveland State University, personal communication, 1979). Ata
depth of 414 centimeters below the lake floor the radiocarbon age is 8250 + 145
years B.P.; between 210 and 228 centimeters the radiocarbon age is 4020 + 190
years B.P. These ages indicate that the deposit was built up during a rising
lake level, possibly the result of a combination of fluvial, deltaic, and beach-
nearshore environments. Aside from the sand deposits, the finer grained sedi-
ments appear, for the most part, to reflect present-day wave and current
conditions in the lake, perhaps largely related to fetch and prevailing winds
as hypothesized by Thomas, et al. (1976).

V. SUMMARY
The southern Ohio waters of Lake Erie (commonly from 1 to 7 kilometers off-

shore) between Conneaut and Marblehead were surveyed in August of 1977 and 1978.
Primary survey data consist of 5/6 kilometers of seismic reflection trackline

40

profiles, taken in 1977, and 58 vibracores ranging from 0.7 to 6.1 meters long,
taken in 1978. About 23 percent of Ohio's part of Lake Erie was covered by the
survey.

Shale underlies most of the survey area. The shale is overlain by glacial
tills and by postglacial deposits. The surfaces of all the units slope lake-
ward. In general, the shale is exposed nearest the shore and succeeded offshore
by till and postglacial deposits. The shale surface is irregular in comparison
with the till and postglacial deposit surfaces and its slopes range from 5 to
20 meters per kilometer. Basal till and flow till were identified in many of
the cores. An olive-gray basal till was found over much of the area and a
yellowish-gray basal till was found in the Lorain-Vermilion area. Some of the
tills contain interlaminated silts and clays (varves?), and three cores contain
both basal till and flow till. The tills are made up largely of silt- and
clay-size particles composed of quartz and illite. The till surface is much
flatter and more uniform than the underlying shale surface and its slopes range
from 1 to 4 meters per kilometer. Overall, the till thickens lakeward at about
5 meters per kilometer.

On the basis of cores and echo character on the seismic records, four
principal postglacial deposits were defined: sand, muddy sand, sandy mud, and
mud. At about 9 kilometers offshore, the stretch from Conneaut to Fairport
Harbor is characterized by postglacial sediment thicknesses ranging from 10 to
16 meters; the stretch from Fairport Harbor to Cleveland is characterized by a
lack of postglacial sediment. At about 5 kilometers offshore, the area from
Cleveland to Lorain is characterized by postglacial sediment thicknesses ranging
from 0 to 2 meters; from Lorain to Vermilion the thicknesses range from 4 to 5
meters. In general, the finest sediment is found closer to shore and in
shallower water west of Cleveland.

The irregular shale surface in concert with the characteristics of the
buried river valleys implies an irregular surface before Pleistocene Glaciation.
The relatively smooth till surface is likely the product of several Wisconsinan
glacial advances and retreats. The physical variations in the till in the cores,
as well as the internal seismic reflectors in the till, indicate that multiple
tills were emplaced. The topographic lows on the till surface off Fairport
Harbor and Lorain-Vermilion imply stream erosion, and the scarcity of glacio-
lacustrine clay implies stream and wave erosion following retreat of the last
Wisconsinan glacier. The postglacial deposits accumulated during a rising lake
level from fluvial, deltaic, and lacustrine processes. The sedimentary deposits
on the lake floor reflect Pleistocene and Holocene processes as well as the
configuration and nature of the underlying rock and till. Present-day waves
and currents tend to erode and rework the shale, tills, and postglacial
deposits in high-energy environments. Subsequent deposition of these sediments
in low energy environments is obscuring evidence of previous low water stages.

4|

LITERATURE CITED

AMERICAN ASSOCIATION OF PETROLEUM GEOLOGISTS, "Seismic Stratigraphy--Application
to Hydrocarbon Exploration," C.E. Payton, ed., Memoir 26, Tulsa, Okla., 1977.

BARNES, B., et al., "Geologic Prediction: Developing Tools and Techniques for
the Geophysical Identification and Classification of Sea Floor Sediments,"
Technical Report ERL 224-MMTC-2, National Oceanic and Atmospheric Administra-
tion, Rockville, Md., 1972.

BENSON, D.J., “Lake Erie Shore Erosion and Flooding, Lucas County, Ohio," Report
of Investigations No. 107, Ohio Department of Natural Resources, Division of
Geological Survey, Columbus, Ohio, 1978.

BOWNOCKER, J.A., "Geologic Map of Ohio," Ohio Department of Natural Resources,
Division of Geological Survey, Columbus, Ohio, 1920.

CARTER, C.H., "Lake Erie Shore Erosion, Lake County, Ohio: Setting, Processes,
and Recession Rates from 1876 to 1973," Report of Investigations No. 99, Ohio
Department of Natural Resources, Division of Geological Survey, Columbus,
Ohio, 1976.

CARTER, C.H., and GUY, D.E., "Lake Erie Shore Erosion and Flooding, Erie and
Sandusky Counties, Ohio: Setting, Processes, and Recession Rates from 1877
to 1973,'' Report of Investigations No. 115, Ohio Department of Natural
Resources, Division of Geological Survey, Columbus, Ohio, 1980.

CROWELL, K., "Ground-Water Resources of Cuyahoga County," Ohio Department of
Natural Resources, Division of Water, Columbus, Ohio, 1979.

DAMES AND MOORE, "Airport Feasibility Study - Lake Bottom Geotechnical and
Geophysical Studies," Reports 5-1 and 5-2, Cleveland, Ohio, 1974.

DREIMANIS, A., "Last Ice-Age Deposits in the Port Stanley Map-Area, Ontario,"
Geological Survey of Canada, Paper No. 70-1, Part A, 1970, pp. 167-169.

DUANE, D.B., ''Sand Deposits on the Continental Shelf, A Presently Exploitable
Resource," Proceedings of the Regional Meeting of the Marine Technology
Society, 1968, pp. 289-297.

DUANE, D.B., "A Study of New Jersey and Northern New England Coastal Waters,"
Shore and Beach, Vol. 37, No. 2, Oct. 1969, pp. 12-16.

EWING, J.1., "Elementary Theory of Seismic Refraction and Reflection Measure-
ments," The Earth Beneath the Sea, Ch. 1, Vol. 3, Interscience Publication,
New York, 1963, pp. 3-19.

FOLK, R.L., Petrology of Sedimentary Rocks, Hemphill's Publishing Co., Austin,
Tex., 1974.

GROSS, D.L., and MORAN, S.R., "A Technique for the Rapid Determination of the

Light Minerals of Detrital Sands," Journal of Sedimentary Petrology,
Vol. 40, 1970, pp. 759-761.

42

GUY, H.P., "Laboratory Theory and Methods for Sediment Analysis," Book 5,
Ch. Cl, Techntques of Water Resources Investigations of the United States
Geologtcal Survey, U.S. Government Printing Office, Washington, D.C., 1969.

HARTLEY, R.P., "Sand Dredging Areas in Lake Erie," Technical Report 5, Ohio
Department of Natural Resources, Division of Shore Erosion, Columbus, Ohio,
1960.

HARTLEY, R.P., ‘Bottom Deposits in Ohio Waters of Central Lake Erie,'' Technical
Report 6, Ohio Department of Natural Resources, Division of Shore Erosion,
Columbus, Ohio, 1961.

HOOVER, K.V., ''Devonian-Mississippian Shale Sequence in Ohio," Information
Circular 27, Ohio Department of Natural Resources, Division of Geological
Survey, Columbus, Ohio, 1960.

LEWIS, C.F.M., "Sedimentation Studies of Unconsolidated Deposits in the Lake
Erie Basin," unpublished Ph.D. Dissertation, University of Toronto,
Ontario, Canada, 1966.

MOORE, D.G., and PALMER, H.P., "Offshore Seismic Refraction and Reflection
Measurements," The Earth Beneath the Sea, Ch. 1, Vol. 3, Interscience Publi-
cation, New York, 1967, pp. 3-19.

MORGAN, N.A., "Geophysical Studies of Lake Erie by Shallow Marine Seismic
Methods," unpublished Ph.D. Dissertation, University of Toronto, Ontario,
Canada, 1964.

PREE, H.L., Jr., ''Black River Basin, Underground Water Resources," Ohio Water
Plan Inventory File Index D-4, Ohio Department of Natural Resources, Division
of Water, Columbus, Ohio, 1962.

SLY, P.G., "Lake Erie and Its Basin," Journal of the Fitshertes Research Board
of Canada, Vol. 33, 1976, pp. 355-370.

SLY, P.G., and LEWIS, C.F.M., "Geology of Lake Erie," The Great Lakes of Canada
--Quaternary Geology and Limnology, XXIV International Geological Congress,
Montreal, Quebec, 1972, pp. 42-50.

STEIN, R.B., "Huron River Basin, Underground Water Resources," Ohio Water Plan
Inventory File Index D-2, Ohio Department of Natural Resources, Division of
Water, Columbus, Ohio, 1962.

THOMAS, R.L., et al., "Surficial Sediments of Lake Erie," Journal of the
Fishertes Research Board of Canada, Vol. 33, No. 3, 1976, pp. 385-403.

TIREY, G.B., "Recent Trends in Underwater Soil Sampling Methods," Special Tech-
nical Publication 501, American Society for Testing Materials, Philadelphia,
Pao, UN

U.S. ARMY, CORPS OF ENGINEERS, COASTAL ENGINEERING RESEARCH CENTER, Shore

Protection Manual, 3d ed., Vols. I, II, and III, Stock No. 008-022-00113-1,
U.S. Government Printing Office, Washington, D.C., 1977, 1,262 pp.

43

VERBER, J.L., "Bottom Deposits of Western Lake Erie," Technical Report 4, Ohio
Department of Natural Resources, Division of Shore Erosion, Columbus, Ohio,
1957.

WALL, R.E., “A Sub-Bottom Reflection Survey in the Central Basin of Lake Erie,"
Bulletin of the Geologtcal Soctety of Amertca, Vol. 79, 1968, pp. 91-106.

WHITE, G.W., "Extent of Till Sheets and Ice Margins in Northeastern Ohio,"
Geological Note 6, Ohio Department of Natural Resources, Division of Geologi-
cal Survey, Columbus, Ohio, 1979.

WHITE, G.W., and TOTTEN, S.M., "Glacial Geology of Ashtabula County, Ohio,"
Report of Investigations No. 112, Ohio Department of Natural Resources,
Division of Geological Survey, Columbus, Ohio, 1979.

WILLIAMS, S.J., and MEISBURGER, E.P., "Sand and Gravel Resources and Geologic
Character of Central Lake Erie - Conneaut, Ohio, to Erie, Pennsylvania,"
MR 82-9. U.S. Army, Corps of Engineers, Coastal Engineering Research Center,
Fort Belvoir, Va., Oct. 1982.

WILLIAMS, S.J., PRINS, D.A., and MEISBURGER, E.P., "Sediment Distribution Sand
Resources, and Geologic Character of the Inner Continental Shelf Off Galveston
County, Texas," MR 79-4, U.S. Army, Corps of Engineers, Coastal Engineering
Research Center, Fort Belvoir, Va., July 1979.

WILLIAMS, S.J., et al., "Sand Resources of Southern Lake Erie, Conneaut to
Toledo, Ohio--A Seismic Reflection and Vibracore Study," MR 80-10, U.S. Army,
Corps of Engineers, Coastal Engineering Research Center, Fort Belvoir, Va.,
Nov. 1980.

44

APPENDIX A
CORE SEDIMENT DESCRIPTIONS

This appendix contains core sediment descriptions, based on both megascopic
and microscopic examinations. Color is based on damp samples as referred to
the Munsell color system (Munsell Soil Color Charts, 1954 ed., Munsell Color
Co., Inc., Baltimore, Md.); grain size is based on the Wentworth size scale.

The marks on the left side of the stratigraphic log are placed at the mid-
points of sampled intervals used for size analysis. The type of analysis is
designated by the following codes (size data are tabulated in App. B):

R

Rapid Sand Analyzer (RSA)
S - Sieve analysis

V Visual Accumulation Tube (VAT)

P - Pipet analysis
The letter B indicates the bottom of the core.

Sediments are grouped into the following six basic categories for logging
(minimum unit thickness shown is 20 centimeters):

=
Sand WY Clay

Muddy Sond

Column descriptions for core sediments are:

Silt

Gravelly Clay

NW = midpoint of sampled sediment used for natural water determi-
nations (interval usually 10 centimeters long); number is:
weight of wet sediment minus weight of dry sediment divided
by weight of wet sediment times 100.

P = penetrometer measurement (in tons per square inch or kilo-
grams per square centimeter).

SV = shear vane measurement (in tons per square inch or kilograms
per square centimeter); PF = plastic flow.

Water depths are the surveyed water depths; these depths were about 1 meter
above low water datum (LWD) for Lake Erie.

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14

APPENDIX B
GRANULOMETRIC DATA AND CUMULATIVE CURVE PLOTS

The samples in this appendix are identified by core number and sample inter-
val below the top of the core. Locations of the samples in each core are shown
in Appendix A.

1. Rapid Sand Analyzer (RSA).

Data include the frequency and cumulative percent at 0.5-phi intervals.
Also included are median, mean, standard deviation, skewness, and kurtosis for
each sample. Experience has shown that grain-size values from RSA analyses are
consistent and slightly coarser than results of sieve analyses of identical
samples; therefore, empirical relations for converting RSA means and standard
deviation to sieve analyses equivalents have been determined. The relation-
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(Williams, Prins, and Meisburger, 1979):

Mean: Xasieve = 1.0735 XORSA + 0.1876

Standard deviation: Opeteve 1.4535 OgRSA - 0.146

2. Sieve Data.

Data include frequency and cumulative percent at 0.5-phi intervals from
samples estimated to have gravel percentages over 10 percent.

3. Cumulative Curves.
Sieve data plotted at 0.5-phi intervals.

4, Pipet Analysis.

Percentages of sand, silt, and clay are included for each sample.

5. Visual Accumulation Tube (VAT) (Guy, 1969).

Percentages of sand and silt-clay as well as mean grain size are included
for each sample.

9

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COTO Cz eNnmt
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Ov*o o7fe01E
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ovuoee (,2) °
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3803

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vuysseq qua) jag ¥ Tuyssed quay 13d
U9) 13d aayzIeTAuNy Wad) 19d aazaeTNuNy
J2aTIeTOUND SSaTaN : DATIeTNUND
——— —————
= 232g 5 ‘hq pozktcuy =°.18 SO°OL oa [deg Jo ay3zay | 23eq = Aq pazkttuy 38 TyOve aTdtes Jo ay3sTzay
| Or, GNVS 4) SISATVKV AAaIS i % GNVS 40 SISATVNV ZAqIS So
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ae = ; ar ere

oo _____ Vd “aruda | ‘ON aTsUrS fof 18907,

OIHO - aldd ANV1 SNOOI 979fo02g | | =e OIHO - dIdda aXNVI . SNODI _929f02g
ZS00 = 9499 | i; 6261 Aen 22eq ‘£q paaraT 109 S00 RI 939

ee oO DTGUTS M07 IBI0F |

Ferer eR 03tg : hq paa221T09

| : SUSMIVNY Lvablids 209 a il ji "EB SUSATVNY LNANLGdS 29

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tal
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oss el
002° 6T
007° 2Z
029°9Z
cussed quay jad ° k qua) Jed W
qua) 13d aazaetauny aoa sed Uda) «ied aazIeTAuND
oAFIe TAN) SoKaTg UO Pousesoy i uaa10$
228g 6 ‘Sq pozfktouy °33 66 6cl a[dres 30 ayszay / 230g 6 kq pozdktouy °18 09° dIT atdres jo wystay
GNYS JO SISATVNV JATIS } GNVS 40 SISATVNV JAGIS
ees a wo SZ 8S au0D S4lenay ae E e m2 = 9s mop «= S4LENaY
= °on DTAUTS P07 18207 y =e See _DTSUS MOT 1BIOT
= “OIHO - a1ua ANVI SNOSI _229f03g Sas OIHO - a1ud ENVI_SNODII22F03g
——— oor? .
6161 Aen 93°d Aq p2a92TT09 gsoo #2 9M3ID | 626 APH 92°C ‘Aq poa2TT09 ; ssoo |= KI NAD

SUSAIVNY InahlGds Qa | SUSAIWNV IndhdS OW

e807 10 UTEy

| Se*tt |
| os" t+ |
| Sz" t+ |

oovT | 0SO-
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Z96" sz*T=

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Zuyssed quay Jag W
qua) -ad aayzaetnung seed e®) Suyuodo
SARI TNUND GahaTS UO Pousers9y uaai2s
a3eq s hq pazh{tuy °38 TS°@tl 2% dres jo aystay
| ; GNVS 4C SISATVNV JARIS
a Z @) y6 - Te 18 mop Sfienay
ae : _Vd ala SOK DTIETES OT 189074
= mam O1HO - aida avi Oo _299f03g
“Aq paasattod 7800 m9 9339

ads ous

Wuyzshed
quag 4ag

DAT IBTNUND

B8OT 10 UTED

i}
t

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mise
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wo
Ga)

TO'IT

66°8T

8°T

002° 6T

-qua) jad

BapseTNuN? Suyuodg

uaa10s

°18

‘ : aug es hq pozfyouy 79 G8 [des Jo 32ySFOy
| ‘ NYS 40 SISATVEV SATIS

(Ez > mw 2-0 TL mu09 S4ienay

' : °oN aTdUCS M07 1BIOF

= ia “OHO - a1ua av SNOoT 299024

| —<°hs0 cq) Gas ‘Aq paarat 109 TL00. -K2 999

SUSATVNY LNINTddS Odd e .

8 |

| Se* tt |
| _os* t+ _|
GEIL AES

~~

68°0OT
007°Z
0L9°9

[=e Tt ]

.9Uua) Jad
aazaetnung

qua9 104
Daz IB{TNuND

—

GzZ°6Tr oTdtes Jo IYy3FaAy

hq pazktcuy °18
GNVS JO SISATVNV ZAqLS

md ce - OF. 06 4000 sulenay
"ON OTGUCS Moy; 18904
—— "STAT = Alda AAVT —SNODT j>9fo3ag
kg paarat Too 0600 K2 099

boom mare
1

| 6L6t Ken o1g

SISATVNY LNINIOdS 29

nett eons mai eee t

Gs0T 10 uyEy

Toes]
oe’y

-d

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[este]

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bal vn

(=)
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Cond (tn! Kent

69° 9T

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CO) 4 -F flr ico
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007° 22
09°92

quay 20g
quo) 36d BAPIETNUAD

DATIVTAUND

| 238g 5 hq pozktruy =°.18 O816l a{Tdtes jo ayszay
1, GNVS 49 SISATVKV 4AqIS

a fe mw 9S - 0S 48 NOD , S¥iEnay

— OX DTAUESPOT IBIOT

a =o "“OIHO = a1ua DWT _SNooT 999 Fo2g

avg : Aq paasaqtoo “Te00 89 OND

TIsATNV ININiGaD owas

(geemceeer mera seoT 10 ure
ee | SSeS LEA
se’ 10

Slit
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a a Ya

Wufssed
_qua9 ted
Day IBTAUND

_ quan 12d

Bay3eTAwND
uaa12

$18 SCOT @¥T =«otdres Jo aystay

anny ¢

‘hq pozktouy

GNVS 40 SISATVNV AALS

08 - SL 06 aWOD S4teney
20% OTAULS Moy B90

O = Alea aiv1 SNOSY | _329foag
0600

camg St™~t~t~CSTCN Gs pv ang TO,

ne BUSMy Wana oS

ee Bao 30 wr#D
a BTe

| ote
[oot it

060°

/ (=)
a k=)
a

feces dS Laie)
asl RSE

Ost’
ESS ees

ares
ae Cees | NOC

ZL YT
RReEaa
Sau

007° 22
0L9°92

Wuyssed

-3uag 12d
qua) 134 BAyIeTAUND gayucdo
DaTIB TAN) uaa13S

ES 22eq s hq pezktcuy °.18 69° 091 odes Jo 3y43Tay
‘| GNVS 30 SISATVNV JAIIS ‘ .

= M3110 9E=105 ge Cp aHOO NE ALET SN

: aS ON aT des Mot B90}

OIHO - ala AXV1 Snood 923034
0600 LP) ow e)

"930g = “hq paadatto9

CERC SRILIEST ANALYSIS

cree ¢__0094 Collected by Date_May 1979 _
Project ICONS LAKE ERIE - OHIO

Location/Saaole So. ERIE, PA Fag,
Rewary.g CORE 94 ~ 100 - 110 cm s:
——

STEVE ANALYSIS OF SAND
Wéighe of Sample_155.15 gr. Analyzed by 2 Date

Cumulative
Per Cenc
Passing

U.S. :
Number

i was 1s bt mre ee eran|

ES ELT

2205 00 | 7/6 NNT

[r=4.00 [19.200] 378
colo. COU nea |minro; mina}

13. a

Screen
Opening
MY

Cumulative
Per Cent

reacoanl 68

=3.50 11.190
9.520

063
0. 000 100

| Po ane
EGYPT Ea WME DTT

84

Percent Coorser

Percont Coorcer

SIZE ANALYSIS

Millimeters

3.50 2.50 1.50 :90 .70 .55 .45 33 .25 AS 09 07
4.0 | 3.20 2.00 | O/.80} .60) 50} 40} .20 : d 4

1
=2.0

eee apes

eq Median ni 75

-I3 -10 -0.5 to) 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0
Pri Units 6

WENTWORTH SCALE

SIZE ANALYSIS

Millimeters
90 .70 .55 .45 35 .28 WS 09 07
0|.80| 60).59| 40) .30 10 | .08 |.

Core 52
- Interval 76-77cm

3 2k TOE te a aa
US Med 0.3
as eA i i io

“1.5 <-10 -0.5 c°) 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0
i Phi Units 6

eranuce | ERY COARSE | coarse sano | weoiuy send | Finesano | “ERI VjNE

WENTWORTH SCALE

85

Percent Coerser

Percent Coarcer

SIZE ANALYSIS

Mlilimeters

55 .45 33
50] .40' .30

Core 56
- Interval 257-260 cm
Medion-<-2

B) 1.0
Phi Units a

WENTWORTH SCALE

SIZE ANALYSIS

Millimeters
:35 .45 .35
50| 40) .30

Interval 25¢
Median + 0.65

2.0 <-1.5 -10 -0.5 2.5

1.0
Phi Units a

WENTWORTH SCALE

86

Percoat Coorces

Pereoat Coarcer

SIZE ANALYSIS

Millimeters 35 A 5 ealuion
H i 1.50 90 .70 .55 .45 ° 2 al d
3 S007" i -00{.80] .60).50] .4¢) .30 d d i

Core 71
20 [a eel Interval 0-7cem
's en Median-0.!5

WENTWORTH SCALE

SIZE ANALYSIS

Millimerers
55 45 .35

Interval 31-34cem
19 Median-0.27

WENTWORTH SCALE

87

Porceat Coercer

Percon) Coarcor

SIZE ANALYSIS

Millimetors
55 .45 35

teh
ivciee fe elem Core

stl 50-54cm
| Wedian-0.4 ¢

s 1.0 :
Phi Units @

WENTWORTH SCALE

SIZE ANALYSIS

Millimeters
2.50 1.30 cies at 55 .45 35 -25 19 09 OF
OF 60) .50| .4 30 : i i

Core 90
Interval 30-35cm
Median-1.6

2.0 <-15 <-10 -0.5 0 0.5 1.0 15 2.0 2.5 3.0 3.5 4.0
Pri alts @

WENTWORTH SCALE

88

Percent Coeroer

Percent Coorcer

SIZE ANALYSIS

Miliimeters
35, 45 !

Interval-50-60 cm
Median -0.8

2.0 <1.5 <-10 -Q.5 t*) 0.5 1.0 1.3 2.0 23 3.0 3.5 4.0
Phi Units §

[_enamvee [ VEREma Se | conse sano [wena sano] rine sano | Y'Siwo |

WENTWORTH SCALE

SIZE ANALYSIS
Milllmeters
35 .45 {-}

Core 90
Interval 75-80cm
Median-I.1

1
2.0 --1.5 -10 -05 O 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0
Phi Units 6

WENTWORTH SCALE

89

Percent Coorser

SIZE ANALYSIS

Millimevers
55 .4

Core 94
Interval 100-I!O0cm
Median —-0.75

|
-2.0 <-15 <-1.0 -0.5 0.5 1.0 1.5 2.0 2.5 3.0 3.5 4.0
Phi ie @

WENTWORTH SCALE

90

PIPET ANALYSIS

360 to 370 °
470 to 480 35.88 52.99 11.13
560 to 570 18.92 42.12 38.96

61/40 to SO 71.0 22.47

6.53
100 to 102 69.7 23.5 6.7 cere ee ares Pere
Peo ee 20 See Ge ora) eee 250 to 260 13.59 46.63 39.78
Rm eaeen cee ee) aaa 285 to 295 10.92 51.93 37.51

. = . 390 to 400 15.77 38.14 46.09

62|70t080 S$.2 57.3 37.5 ‘ 10,52 38.35 51.13

160 to 170 26.8 58.46 16.8 480 to 490 4.08 26.14 69.78
{

20 te 330 61.62 25:43 12195 99 600 70 2.65 75.76 21.61
| ta. . 6 . °

63/50 to 60 8.38 60.91 30.71 270-+0-280 0.66 68.64 30.70
220 to 222 69.7. 17.9 «12.4 915 to 325 19.20 44.45 36.35
450 rr Un eee 99 30 to 40 | 2.12 75.88 22.00

° 0 0 100 to 1100.26 «68.43 31.31

66 | 60 to 70 2.21 61.05 36.74 250 to 260 16.85 42.88 40.27
150 to 160 29.01 46.55 24.44 310 to 320 39.80- 57.72 - 2.48
226 to 226 ©8.02 57.65 34.33 ; 5
350 to 360 «5.31 59.15 35.58 101 553 to 55672 25 2
450 to 460 «3.83 52.89 43.28 102 OQtoS 25 51 24

67 40 to 5u 61.59 25.02 13.4 i to a 3 a ;
170 to 180 =«51.7 30.7 ~—-17.6 aaa eo) ap 8 ri xn
1260 to 270 ©=«1.56 49.09 49.35 Sr ere lg aa
360 to 3701.1 54.6 44.5 te. 36
460 to 470 1.07 38.57 60.36 103 - 460 tm 143.6 92 2

69 250 to 260 72.86 17.40 9.76 Pe rea 33 F
340 to 350 © 53.29 34.98 ~=-11.73 oe ome. 5 a 3
440 to 450 2.66 52.68 © 44.66 Ao ay OH a 5
540 to 5500 1.37. 49.2 49.43 ce

72 10 to 20 7.96 80.21 11.83 ai rene sont iige
165 to 66 18.43 61.62 19.95 oe GD a | ea 73
150 to 160 11.77 62.02 26.21 neh co ww 8 aa at
340 to 350 0.34 51.82 47.84 Te5 S TORS bs 2

74 | 20 to 30 5.7 29.0 65.3 202 to 206 = & 80 16
285 to 295 5.7 26.0 68.3 300 to 305s tt 63 37
470 to 480 «1.7. 47.6 50.7 Sapna Ly Re 0

77 100 to 110 14.42 54.96 30.62 50 to 80 58 39 3
525 to 535 18.01 41.08 40.91 99 to 104 15 81 4

79.600 63 32.05 49.8 18.15 ee ae iB
105 to 115 21.66 940.1 38.24 Ee = To 66 34
300 to 310 4023.26 «39.66 += 37.08 aa = nO 6 2

81 200to 210 «1.1 73.5 25.4
310 to 320 «0.8 Ss 465.8 53.8 TOS i iysnes SOB 38 2 2
400 to 410 11.8 37.7 50.5 seni ca on G oO he

83 60to 45 20.95 52.54 26.51 354 to 3597 52 AE
100 to 110 «=. 2.53. 71.18 26.29 626 to 6299 69 42
475 to 485 2.05 60.50 37.45 ro Ago 1 estas

84 250 to 260 30.35 67.86 1.81 33 to 36042 57 1
335 to 365 16.60 40.16 43.24 70 to 80 «65 35 0

85 100 to 110 11.79 71.91 16.3 waigasoee 138 Terns :
370 to 380 «= «46.18 +««77.64 +=—«16.18 Pen cates a a
405 to 415 15.30 37.85 46.85 eR me

86 | 90 to 100 16.61 73.32 10.07
240 to 250 15.84 41.02 43.14

ltrace amount.

VISUAL ACCUMULATION TUBE (VAT)

INTERVAL >4 phi. <4 phi' MEAN STANDARD ©

Core (cm) (pet) (pet) bi DEVIATION
101 45 to 60 84 16 3.9 0.7
130 to 140 82 19 3.8 0.6
180 to 200 91 9 3.6 0.6
103 0 to 5 98 2 2.8 0.7
106 7 to 10 95 5 Sait 0.7

Sil

APPENDIX C

X-RAY DIFFRACTION ANALYSES

g2

x

* x

*
~~ MS KM OM

<

T*

taket
POXFW | F3F UT TORY

(1eeus) uozIIeAZ WN Z> STeAeUTU AeTOD

xX xX
xX xX
X xX
xX xX
xX xX
xX xX
x x
xX X
x X
X xX
X xX
xX xX
xX xX
xX xX
xX ¢
xX xX 12 0 oT 8T TY
X xX £Y (al 82 €Z LS
X xX xX €e €T Ov 02 £6
» 4 xX 8T 9T 4 8T 6S
X xX 1x £9 0 ce oT 82
Qa TNoFWIaA | ayFUOTTTA aseTo | 1edspTez | (67,99°0Z)
eIFIIL —9 3}; 10TYD -owjuoW | ayFWOTOG | eIFITeD | -oF3e Ta ysejod z31enh

aUTT 28Seq eAoge sat jTSuequT yeed

un > Sjunow IPoauUs

“@TBIS F50¢
‘Jusseid qunowe iouzu = ¥z
*qQuosoid = Xy
(L) Aeqto
ATT eae1g 90T
(d) IT¥S 90T
(1) 4eT9 401
(1) Aeto
ATTeaei9 66
(1) 4eTo 66
(d) TFS 66
(L) Aeqo
ATTeaesg G6
(d) 3TFS 66
(d) 31S G6
(d) 31¥S G6
(L) Aeqto
AT pTeae1y "8
(L) 4eqto
ATTeAe19 LL
(d) 3TFS LL
(1) Aeto ZL
(1) Aeto ZL
(1) eto
REC OT*z ATT eaei9 19
7L°0O 8c°0 (d) ITS 19
07°0 82°0 (d) 3T¥S 99 19
(L) Aeqo
9S°T ToT “AT Teae19 Oy cs
(d)
S70 9€°0 pues Appny SOT SS
Zeb S| ae
/23440TUD
+ a3FUT TORY
(TeFoeT3 (e109
Sta = 1) woij wo) “ON
TepszeseW TeArejuy | 8109

93

Core
No.

op)
60
61
61
61
72
72
74
74
77
79
79
81
81
84
85
85
85
86
95
96
96
98
My)
99
105
105
105
105

Interval

(cm from top

of core)

398
560
190
280
310

70
340

10
470
200
100
300
310
400
335
200
370
400
230
430
285
480
316
240
305
130
310
370
440

to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to
to

to

420
580
200
290
325

77
347

25
490
220
72)
320
320
410
350
210
380
420
250
445
295
490
325
255
320
140
320
380
455

APPENDIX D

ATTERBERG LIMITS

Material
(T = till;

2S

Gravelly
Gravelly
Salle (G2)
Sslten@B))
Gravelly
Clay (T)
Clay (T)
Clay (T)
Clay (T)
Gravelly
Gravelly
Gravelly
Clay (T)
Clay (T)
Gravelly
Saat GB)
Silt (P)
Gravelly
Gravelly
Gravelly
Gravelly
Gravelly
Gravelly
Clay (T)
Gravelly
Site) (PR)
Sallis (02)
Gay (2)
Clay (T)

postglacial)

clay (T)
clay (T)

clay (T)

clay (T)
clay (T)
clay (T)

clay (T)

clay (T)
clay (T)
clay (T)
clay (T)
clay (T)
clay (T)

clay (T)

94

Liquid
limit
(pct)

28

Plasticity
index

10

Oe Oe)

26
2.

APPENDIX E

MOLLUSK IDENTIFICATIONS FROM CORES

1

Abundance
Phylum - Mollusca
Class - Bivalvia
Order - Prionodesmacea
Family - Unionidae
Genus - Elitptio
E. dtlatatus sterkit -
Subfamily - Lampsilinae
Genus - Lampstlis
L. radtata =
Lampstlts radtata stliquotdea -
Genus - Obliquarta
Obltquaria reflexa -
Order - Teleodesmacea
Family - Sphaeriidae
Genus - Sphaertum
Sphaertum sp. +
Class - Gastropoda
Order - Ctenobranchiata
Family - Amnicolidae
Genus - Amnicola
Amntcola integra +
Amnteola lacustris +
Amntcola letghtont +
Amntcola limosa +
Amntecotla sp. +

Subfamily - Lithoglyphinae
Genus - Somatogyrus
Somatogyrus subglobosus -
Subfamily - Bulimnae
Genus - Bultmus
Bulimus tentaculatus 0
operculum from Bulimus tentaculatus -
Family - Pleuroceridae
Genus - Pleurocera

Pleurocera acutum 0

Pleurocera sp. 0
Genus - Gontobasis

Gontobasts ltvtseens 0

Gontobasts haldemant 0

Family - Valvatidae
Genus - Valvata
Valvata sincera +
Valvata trtcarinata +
Family - Pomatiopsidae
Genus - Pomatiopsts
Pomatiopsts laptdarta =

laAbundance: + is abundant; O is common; - is rare.

95

Order - Pulmonata
Family - Lymnaeidae
Genus - Fossarta
Fossarta parva
Fossarta modicella rusttca
Fossarta cf. extgua
Family - Planorbidae ©
Genus - Gyraulus
Gyraulus paryus
Subfamily - Planorbulinae
Genus - Promenetus
Promenetus exacuous
Promenetus umbtltcatellus
Family - Physidae
Genus - Physa
Physa gyrina
Family - Valloniidae
Genus - Vallonia
Vallonia costata

labundance: ‘+ is abundant; O is common; - is rare.

96

Abundance

1

APPENDIX F

SEDIMENT THICKNESS DATA FROM SEISMIC RECORDS

Seismic velocities:

water v = 1.54 meters per millisecond
postglacial sediments v = 1.3 meters per millisecond
till v= 1.8 meters per millisecond

Water depth is survey water depth (about 174.3 meters), which is 1 meter above
low water datum (IGLD, 1955).

a. Postglacial sediment and till thicknesses were measured at two con-
fidence levels. Those followed by an "a" (the first confidence
level) are those in which the reflector was well defined on the
seismic record; unmarked thicknesses are those in which the reflec-
tor was not well defined on the seismic record yet whose position
could be reasonably well inferred from the overall geologic setting

and character of the reflector.

b. The letter "b" indicates thickness data not available because (1)
both postglacial sediment and till thicknesses could not be meas-
ured because of difficulty in interpreting the seismic records
(in this case water depth was not measured), or (2) the seismic
reflection record for the fix is missing.

All thicknesses in meters

T = trace of material, <0.5 meter, but enough to change surface echo
character.
x = thickness not measurable because of lack of lower reflector.

on

Fix Water Postglacial Till Fix Water Postglacial Till
No. depth sediment thickness No. depth sediment thickness
thickness thickness

483 13.6 ) 9)
375 to 386 b Aya AS D5 x
388 10.1 0 0 486 15.0 4.0 x

“er? tals 550 x
389 to 422 b 488 15.5 6.0 x
hoe} | Go) 45a 5.0a 489 16.4 7.5a 55

490 16.9 8.5a x
424 15.6 20a 6.0a

491 16.6 9.0a x
G25 1550 2.0a 4.0a
IDA WWALS 2.5 0 OD |) i197) 3} 10.5a x
427 Ana iL (0) 0 493 17.7 10.5a x

: 494 17.8 11.5a x

ON © S58) 0a 0a

“495 elias 25a x
AMG) iL} 0a Oa
430 8.9 0a Oa 496 18.6 12h 5a x
Ae WD f 0a Oa 497 19.0 12 65a x

498 20.5 14.0a x
UBD 13}. Oa Oa
ADS) WANT) 0 LS 499 20.9 15.0a x

SOO M20n5 16.0a x
ingyA 1520 1.0a 6.5a

SOimw 62056 16.0 x
A253 1565 3.0a 5.0a

502 a a2 s 17.0 x
436 16.8 4.5a 4.5a

508. 218 17.0 x
Gyo O 5.0a 9.5a

504 DULG 70 x
438 16.6 5.5a 13.0a

505 DD 17/0 x
439 16.8 6.0a 13.5a

506 22.6 17.0 x
440 16.6 7.5a 12.5a

KO, QQ 17,5 x
Ne 170 7658 12.0a

508m 2216 17.0 x
442 U7 oa 7.0a 12.0a

SOOMAN2 200 17.0 x
haps pe apnea BIO oINe 17.0
444, 16.9 4.0a 10.0a ° ; 28
(HAG) aaa 3.0a 9.0a Sill eo Sel b
446 15}5.8} 3.0a 6.0a 532 15.6 pie ai
447 14.8 2.5a 3.0a

G3) 1665 8.0a 2.0a
448 14.2 1.0a ILS DE)

Rye 1740 8.0a 15a
MES) ID 0a Oa

eI Go 6.5a 3.0a
450 10.4 Oa 0a

536 16.2 5.5a 2.0a
AR 12, 0a Oa

Rey) 1S 3.5a 2.0a
AGH | WWAS7) 0 0

SS Oman 3.5a 1.0a
453 15.0 1.5 x
454 16.0 245) z 939 «14.5 3.0a 1.0a

BVA)! a1), aL Oa 0a
G55. 155 5.0 6.0

Gril |) alah, 0a Oa
456 16.2 6.0 703

542 8.0 Oa 0a
457 16.8 8.0 9.0

543 8.8 Oa 0a
458 16.9 8.5 x
459 16.3 8.5 5 544 11.7 0a 0a
460 16.7 8.5 i AIS) DA 1.0a 0a

546 13.8 1.5a 0.5a

Fix Water Postglacial Till Fix Water Postglacial Till
No. depth sediment thickness No. depth sediment thickness
thickness thickness

Gay Be ese 2.0a 5o7 0) 2405 Tse 91.5a
548. 15.2 2.0a Ase BO | DIG 9.5a Das

5490 015.5 2.0a 2.0a BOQ) Dia 12.0a 19.5

550) 115.8 2.0a AL Ba 600 22.0 12.5 25.0

BL 1548 2.0a Bese 601 22.3 ofa 23.5

BSD aos) 2.0a 5.5a 602 22.1 13.54 23.0

BRS iLyys) 2.0a 9.0a 603" 219 13805 21.0

BBA AD 2.0a 8.0a BOs DILLG 12.0a 18.5

S550 n1G.0 AOA 5.0a GOR BLE 11.0a 16.0

BSG 5.3 2.0a 2.5a GOS. Binal 10.5a ALB
557 |) Bho Se 2.0a GOT ate onan anos
BS ta e7 Oa Oa 608 20.8 8.5a 10.5a
559. 12.0 Oa Oa 609" 2015 8 (5a 8.5a
S600 L107 Oa Oa Glu) HlgiG 8.0 8.5

SQL | BLO Oa Oa ail, | e438) 75 7.0

5628 E1005 Oa Oa Gime loys 78S 3.5

BGS Tale 0a Oa lS 1th 7.5 0

BGA alsigs 0.5 0 Als 165 6.0 0

5650) 1309 2.0a 1.0 6S 17d 5.5 0

Bas WAG 2.0a 1.5 Blom lene 8 0

B67 ISAO 2 Ba 2.0 Ain WSS 3.0 0

56eN 16.2 2.58 2.5a AG Wail 2.5 0

BGO 11Go8 2.5 2.5 AO 13.6 1.5 0

STO aT <3 2.5 5.5 E2O. 18.48 Oa Oa
By | oy 2.5 7.5 Gi) sae? T 0

572 1850 215 9.5 A NOLO T 0

573 1.0) AOE 8.5a 623% 1007 T 0

Baise 3.0: 10.0a nh 18.0 T 0

575 17.6 2.5a 6.5a

BIG ies 3.0: BOA 625 to 636 lB

B77 IGoe 2.0a Shon A571 AO T 0

578 15,8 1 Sa aoe Bx ilalos Oa Oa
By) 1553 ese Lo Se 639m) oo 0a Oa
580 14.2 on Oa COM NIenS Oa Oa
Boe a2 Oa Oa Gaia) 192 0a Oa
582 10.0 Oa Oa 6404) |acines Oa Oa
55 GA5 Oa Oa GASH i MALLS Oa Oa
584. 8.9 Oa Oa Gil | DLA T z
598. ililey 0a Oa

BSG. Sul Oa Oa ER2 eo O30 0

SG7 | Bez 2, Be Oa 6ST se oe 0

BE | aSiKG 3.0a Oa QBS TLAG 2.0a 0

B30 746 3.5a 3.02 G5om ene 2:0a 0

590 18.8 A On 5.0a 260. Bie 2.0a 0

591 18.2 A Se er ay.) Oar ise 0

592 19,1 55a 8.0a 66m ONG ise 0

GOS 2Osil Glos 10.0a 663 | 1O.S 2.0a 0

594 20.7 ans iON AGA HOLE ise 0

595 20.9 TOA 13.0a 465 TLL na5e 0

BoGn e2a 2 8.0a 14.0a Ran, Mabey 165a 0

99

Fix Water Postglacial Till Fix Water Postglacial Till
No. depth sediment thickness No. depth sediment thickness
thickness thickness

667 10.8 3.561 0 745 17.9 4.0a 9.0
668 10.4 5.0a x 746 17.5 85 SE 10.0
669 10.8 4.5a x 747 17.4 2).5a 10.5
670 11.8 4.0a x 748 Iya T 113} @)
671 12.9 3e5a x 749 16.6 Th 13.0
672 13.0 4.0a x 750 16.6 ap 1265)
673 1263} 5.0a x 751 16.2 T Li, 5
674 13}4,0) 5.0a x 752 14.9 Tk 11.5
675 16.3 4.0a x 753 15.8 0 10.5
754 14.7 0 O55
Oto ete) 7 755 Ay 0 8.0
706 9.6 1 35a x 756 14.4 0 7.0
707 10.5 1.5a a 757 12 67 0 6.0
708 11.0 1.5a x 758 11.8 0 555
709 11.0 1.5a x 759 LIL @ 0 4.5
710 11.4 2.5a x 760 8.8 0 5.5
711 12.0 Zea x 761 7.0 0 555
712 1265) 2.0a x 762 8.2 0 5.0
713 125 7/ ia x 763 9.7 0 x
714 13.4 1.5a x 764 10.4 0 x
715 14.0 loa x 765 11.3 0 x
716 14.3 2.0a x 766 11.4 0 x
717 14.9 Zava x 767 10.9 0 x
718 E50 2.0a x 768 eS 0 x
719 15.0 dea x 769 OD 0 x
720 15.6 20a x 770 343) 0 x
Veal 14.9 4.5a x 771 SoA. 0 x
722 16.4 5.0a x 772 13.5 0 x
723 16.2 6.0a x 773 14.5) 0 5
724 18.0 6.5a x 774 13.8 0 x
725 18.5 8.5a x 775 TA aL 0) x
726 19)53} 11.0a x
Ta) Day 12.0a x 7176 E
728 20.6 12.5a x Wh 14.9 0 10.0
729 Dilos) 14.0a x 778 14.4 0 8.5
730 Dio ® Oa x 779 13} 42 0 8.5
Youk 21.6 6eDa x 780 S62 0 7.5
V3 Pil ots} U7 5 Sel x 781 12.1 (0) 7.0
W333) 22M Wee x 782 i 63 0 6.0
734 Pella ts 17 5 Se x 783 10.7 0 555
735 Dale), 17.0a x 784 9.0 0 4.0
736 Dich 16.5a x 785 6.5 0 3.5
U3i7/ Deen 15.0a x 786 8.4 ) 3.0
738 20.7 14.0a x 787 11.4 0 6.0
739 Oa} lie a x 788 12.8 0) 6.0
740 19.8 10.0a x 789 17256 0 6.5
741 IG). 5) 8.5a x
742 19.2 156 _ U9 20, TOE e
743 19.0 64 Se! x 792 V2 62 0 7.5
744 18.7 HOA 9.5 793 IB sZ 0 6.5

100

Fix Water Postglacial Till Fix Water Postglacial Till

No. depth sediment thickness No. depth sediment thickness
thickness thickness
TOR) ae) 0 9.5 BAS 17.8 0 sg
708. 146 0 120 Sale NG 0 x
706 WAG 0 14.5 845 18.0 0 _
Toy. alAyA 0 x BAG 13,8 0 53
193 WALG 0 x 847i asco T x
799 15.8 0 x B48 les T x
800 14.9 0 x 849 16.9 0 _
Sole 615.5 0 15.0 8500) lene 0 5
802 15.7 0 16.0 851 16.9 0 sg
803 16.7 0 16.5 BED G6 0 sg
S04 e173 0 170 O55 166 0 _
805 17.8 0.5a 18.0 BGA 16.0 0 5g
806 18.0 0.5a 19.0 B55) valons 0 x
B07 Bas T x 856 15.0 0 5g
808 18.7 ean 19.0 O57) WAL 0 x
858 13.9 0 55
oO . 859 13.6 0 53
810 19.0 Tai G08 AGO 13)45 0 x
Sy Wea Onsa 17.5 BG 12.8 0 5g
Sion 0118.6 0.5a 178 B62 1263 0 x
Bg 1A 0 16.0 863 110.2 0 :
814. 18.0 0 16.5 BG, 7.8 0 x
815 17.8 0 15.5 B63 Bo8 0 x
BiG iyee 0 14.5 BEG WOW T 5
Si aee7).0 0 13.5 B67) 1D? T sf
M9 WGs9 0 12.5 868 13.2 T 55
819 16.3 0 12.5 AE WhO 0 55
820 15.8 0 12.0 370 1a.3 0 5g
Bonet (115) 0 10.5 ST ashe 0 x
B000e 14.3 0 LiL 4 872 1500 0 x
B03, WALD 0 9.5 375 18,8 0 5g
8240 o13).6 0 8.5 eyes 15,8 0 x
825 12.5 0 8.5 B78 WSLil 0 iz
826 912.8 Oa 7.0a B76 14,0 0 x
Bp ALG 0a 5.0a B77 1942 0 x
828 1OLG Oa 3.0a B78 | 165 0 :
B2on NSLS Oa Oa B79 18,0 0 y
830 8.8 Oa Oa 880 12.8 0 x
Aa | ss T 2.5a EGIL TALS 0 xx
B32 1265 T x 882 11.4 0 55
833 13.8 T x B83. 12 0 ”
Bak WALD 0 x Seuue loNG 0 x
893. als 0 x 885 13.0 0 _
B36. WALD 0 x SB GmmnanG 0 x
837 b 887 13.5 0 x
838 16.2 0 sg E59 deo 0 x
E39 1664 0 55 BBO Sos) 0 x
GA WGL6 0 55 890 15.1 0 x
Svar allay 43 0 xR 891 15.0 0 x
V2 16.9 0 xz 892 15.0 0 x

101]

Fix Water Postglacial Till Fix Water Postglacial Till

No. depth sediment thickness No. depth sediment thickness
thickness thickness
893 15.0 0 x 942 14.9 1.0a 23.0a
894 15.0 0 x 943 W369) 0 22.0
895 ALS), at 0 x 944 12.6 Oa 18.5a
896 14.3 0 x 945 11.6 Oa 10.5a
897 13.6 T x 946 8.4 Oa 0a
898 13.5 at x 947 67) Oa Oa
899 12.0 a x 948 6.8 Oa 0a
900 10.4 0 x 949 8.7 T 9.5
901 7.0 0 x 950 9.0 T 11.0
902 Uce 0 x 951 10.6 T 10.0a
903 10.6 T x 952 10.7 0 15.0
904 WAG T x 953 11.4 0 17.5
905 12.8 T x 954 ILA Gal 0 20.0
906 610.9 0 x 955 13.6 1.5a 18.5
907 10.0 0 x 956 14.6 1.0a 17.5
957 15.0 1.5a 20.0
2ge 958 14.5 1.5a 21.0
909 8.3 T x 959 15.0 1.0a 2300
910 10.0 T x 960 152 1.0a 23.0
Qala ALLS T x 961 15.8 1.0a 22.5
912 13.6 0 x 962 1562 1.0a 22.5
913 L349) 0 x 963 15.0 1.0a 23.0
914 14.5 0 x 964 14.5 1.5a Peo)
915 14.8 0 x ‘965 14.0 1.5a Dd od
916 15) 42 0 x 966 13.5 1.0a 20.0
917 15.6 0 x 967 13.0 1.5a 7 oS
918 15.8 0 x 968 12.0 1.5a 17.5
919 15.6 0 x 969 iS} 1.0a 15.0a
920 15.8 0 x 970 10.6 1.0a 1.5a
921 15.6 0 x 971 5.8 Oa Oa
922 15.4 0 x 972 6.8 Oa Oa
923 15.4 0 x 973 10.8 1.0a 6.0a
924 1) 55) 0 x 974 11.8 1.5a 14.0a
925 ILS yats 0 x 975 12.8 1.5a 18.0
926 15.5 0 x 976 eS Fay, 2.0a 19.0
927 15.5 0 x 977 U3 SZ 1.5a 19.5
928 1355) 0 26.5 978 14.4 1.5a 20.0
929 14.1 0 25.0 979 14.9 1.0a x
930 WAG 7) Oa 26.0a 980 Noyes 1.0a x
9B 11.7 Oa 14.0a 981 1L3)522 1.0a x
932 4.7 Oa Oa 982 14.8 1.5a 20.5
933 10.9 Oa Oa 983 14.2 1.5a 20.0
934 12.7 Oa 16.0a 984 13.8 2.0a 18.0
935 14.0 1.0a 23.5a 985 13.0 2.0a 18.0
936 15.4 1.0a 25.0a 986 12.4 2.0a 16.0a
937 9 Oa 26.5a 987 11.4 2.0a 12.0a
938 I{)\58} Oa 25.5a 988 10.9 1.0a 8.0a
939 16.4 Oa 25.5a 989 8.3 Oa Oa
940 16.2 Oa 25.5a 990 8.1 0 3G)
941 1L5)55) 0.5a 24.5a 991 8.4 0 5.0

102

Fix Water Postglacial Till Fix Water Postglacial Till

No. depth sediment thickness No. depth sediment thickness
thickness thickness
Oa Oa
Oa Oa
0 0
1.5a 0
1.5a 4.0a
1.0a 7.0a
1.0a 11.5
1002 14.9 al x 1052 14.1 1.0a S}35)
1003 15.5 1.5a x 1053 14.8 0.5a 15.0
1004 15.9 1.5a x 1054 14.8 0.5a 18.0
1005 15.8 1 SE} x 1055 14.2 0.5a 17.5
1006 15.2 1.5a x 1056 13.8 1.0a 15.0
1007 15.2 T x 1057 13.6 0.5a 12.5a
1008 15.2 T x 1058 13.0 1.0a 7.0a
1009 14.6 T x 1059 12.0 Oa 5.0a
1010 1357 T x 1060 10.9 Oa 3.5a
1011 ile 2yepl! T x ! 1061 10.1 0 0
1012 9.0 a Oa 1062 7.0 0 0
1013 9.2 0a Oa 1063 8.9 0 T
1014 9.5 Oa Oa 1064 10.0 0 x
1015 13.3 Oa Oa 1065 10.3 0 x
1016 15.7 1.5a 3.0a 1066 11.5 0 x
1017 16.0 1.5a 8.0a 1067 11.8 0 x
1018 16.2 1.5a 11.5a 1068 ike) 0 14.5
1019 17.0 joa 15.0a 1069 12.5 0 20.0
1020 17.0 1.5a 16.5a 1070 12.9 0 20.0
1021 W710 1.5a 15.5a 1071 12.8 0 2D
1022 17.0 1.0a 15.0a 1072 58) 0) 2259
1023 16.5 1.0a 13.5a 1073 14.4 0 20.5
1024 16.0 1.5a 12.0a 1074 159 0 21.0
1025 15.4 1.5a 7.5a 1075 16.6 0 22.0
1026 aS yey2, 1.5a 1.5a 1076 16.8 1.0a 21.0a
1027 14.5 Oa Oa 1077 16.8 ee) x
1028 11.8 Oa Oa 1078 17.0 5.0 x
1029 10.4 Oa Oa 1079 16.8 6.5 x
1030 11.1 Oa Oa 1080 18.5 365 x
1031 26S) Oa Oa 1081 16.5 Dod) x
1032 14.2 1.5a Oa 1082 16.2 WEE) x
1033 14.5 1.5a 2.0a 1083 16.0 B67 x
1034 15.0 1.0a 8.0a 1084 15.8 3.0 x
1035 15.5 1.0a 11.0a 1085 15.5 Dye x
1036 15.9 1.0a 13.0a 1086 15.0 5.0 x
1037 16.0 1.0a 13.5a 1087 15.0 3.0 x
1038 16.2 1.0a 16.5a 1088 14.8 Jed x
1039 16.2 1.0a 15.0a 1089 13.8 Ge) x
1040 16.0 1.0a 14.5a 1090 13.8 6.0 x
1041 15.2 1.0a 13.0a 1091 14.5 4.8 x
1042 14.8 1.0a 9.0a 1092 15.5 4.2 x
1043 14.2 1.0a 4.0a 1093 15.7 4.8 x
1044 13.8 1.0a 1.5a 1094 16.1 4.5 x

103

Fix Water Postglacial Till Fix Water Postglacial Till
No. depth sediment thickness No. depth sediment thickness
thickness thickness

1101 to 1105 b WSS andelws4 e
TMOG A ELS 0a 6a 58 HSS BLS Oa Oa
ion e) ee 0a 9.5a 15 856 Ox 0
1108 WAS Oa 9.5a WaSy7/ 8.5 Oa Oa
M09) Be 12.3 0 x 1 85 Oa Oa
LG 12,6 0 x MIS) | O60 Oa Oa
Talay G1 DSS 0 x Ga | it. Oa Oa
es | 1D 0a 13.5a AGH | 8 1.08 1.5a
Aisy ee Lae 7 Oa 10.0a iGo 1D. 2.0a 208
aA Gil GS Oa ioe 11S. 19,2 3,06 5.0a
LS 10,2 Oa 6.0a 1164 12,2 3.5a 5.0a
1116 9.1 Oa 5.5a 1165 1255) 4.5a 7.0a
To) Oa 45a WIGS 12,8 45a 8.0
1 YEG Oa 3.5a G7 12.6 5.0a 9.5
Ml 7.9) Oa 3.5a TGS 12.6 5.0a 9.0
1120 «9.4 Oa 5.0a 1iG® 12,5 fs 86 9.0
no GORA Oa 6.0a TO 140 ROA 7.0a
LDA Ta ® Oa 8.5a Ty, ee 332 5.0a
DS DAT Oa 9.5a ya | askee 2 SA 35a
TIN 518\85) Oa 10.0a 7 | LL 1A 1.02
HAS 134 0.5a 10.5a 1174 «9.2 Oa Oa
1126 13.5 ea x 1175 9.0 0a Oa
DT LALO 2 .0a x ins A Oa Oa
1128 14.2 3.5a x
1129 14.5 4.0a 53 1177 b
iO WAL 2 .5a 9.5a 17 THO 1.0a Oa
Hig 13,5 2.0a 9.0a 1i7® | LAO 1,5 Oa
132 19,9 1 SA 10.0a 1180 10.8 ios Oa
1S 132 LSA 8.5a HBL LOL0 0.58 Oa
ney 51S 1.5a 6.0a ig ono 0 0
1S 1,5) 1.0a 5.548 11S BoB 0 0
MSG D3 1508 1.548 Tuy 78 0 0
AS | BLS 0 3.0
1137 and 1138 b fee ei ene ; es
1139 ~=-9.0 Oa Oa i SB 0 0
Mi) Oa Oa Oa 1S B45 1.0 4.0
A 15,5) Ta Oa MSO) | OLO 1.0 4.0
ip) pe On 0 HOO 1) OL0 1.3 2.0
143 128 DAWA 0 dekoa hy OS 1.0 sx
Mian nonS 3.0a 4.0a 11D GLO 1,6 Se
eS 136 4.0a 6.58 AiosiD ens 0.5 x
TIGA BAO 1.0 z
IA 10S) 7S 1.3 52

Fix Water Postglacial Till Fix Water Postglacial Till

No. depth sediment thickness No. depth sediment thickness
thickness thickness
1196 7.0 1.0 x 1246 15.5 2.5a x
1197 14.3 3.0 x 1247 5s)5) 3.0a x
1198 13.7 3.0 x 1248 15.6 3.0a x
1199 12.8 3.5 x 1249 15.8 3.5a x
1200 W263) 2.5 x 1250 15.5 3.5a x
1201 13.9 1.0 x 1251 15.5 2.5a x
1202 14.4 1.0a x 1252 15.5 2.5a x
1203 14.9 1.0a 25.0 1253 VSD 1.0a 25.0
1204 14.8 1.0a 25.5 1254 14.8 T 28.0
1205 15.1 0 25.5 1255 14.4 0.5a Doe)
1206 1567 0 25.5 1256 13}55} 1.0a 28.0
1207 15.2 1.0a 24.5 1257 13.4 0.5a 28.0
1208 15.2 1.5a 23.0 1258 14.3 0 27.0
1209 15.3 2.5a 23.0 1259 14.5 0 27.0
1210 63} 2.5a 22.5 1260 14.5 0) 27.0
WAAL 15.4 3.5a 22.0 1261 14.7 0 27.0
1212 15.6 3.5a 22.0 1262 14.5 0 27.0
1213 15.5 3.5a x 1263 14.7 0 28.5
1214 15.4 4.5a x 1264 14.7 0 BU sd
1215 16.2 3.5a 21.5 1265 13.7 0.5a 27.5
1216 16.2 4.0a 2A 1266 14.9 1.0a 28.0
1217 16.0 4.0a 22.0 1267 15.0 1.5a Bic
1218 16.2 3.5a 21.0 1268 15.3 1.0a 26.0
1219 16.2 3.5a 21.0 1269 15.5 2.0a 25.5
1220 16.0 2.5a 22.0 1270 15.7 1.5a 26.0
NAA AL S59) 3.0a 23.0 1271 15.9 2.0a 25.0
DVD 15.8 2.5a 23.5 1272 15.8 2.0a 24.5
1223 ID6 2 2.5a 23.0 1273 16.2 2.0a 25.0
1224 1L5}.58) 1.5a 24.0 1274 16.3 2.5a 22.5
1225 15.6 1.5a 24.0 1275 68) 2.5a 25.0
1226 15.6 1.5a 24.5 1276 15.5 2.0a 25.0
W227) 15.6 1.0a B05 1277 15.6 2.0a 25.0
1228 15.0 0.5a 25.0 1278 15.5 1.5a 25.5
1229 14.9 0.5a 24.5 1279 15.6 1.5a 25.0
1230 15.0 0.5a 26.0 1280 14.8 1.5a 27.0
WAS AL LS} gat 0 26.0 1281 14.6 1.0a 26.5
1232 14.9 0 26.5 1282 14.1 1.0a 26.5
1233 14.7 0 26.5 1283 14.0 1.0a 28.0
1234 14.8 0 28.0 1284 13.9 0.5a 28.5
1235 14.2 0 26.0 1285 14.3 Oa 28.0
1236 14.1 0 25.0 1286 14.0 Oa 28.0
1237 14.3 0 26.5 1287 14.7 Oa 2 oS)
1238 13.6 0 26.5 1288 14.9 Oa 27.5
1239 13.3 1.0a 27.5 1289 14.2 Oa 27.5
1240 13.1 1.0a 27.0 1290 14.8 Oa 27.5
1241 Boal 1.0a 26.5 1291 14.2 T 240 6
1242 i13},9) 1.0a 27.0 1292 14.6 T x
1243 14.2 1.0a 26.0 1293 13) ,9 T x
1244 15.0 1.5a 25.0 1294 13.3 T x
NS) LS)o3) 2.0a x NDE AG T 26.5

105

Fix Water Postglacial Till Fix Water Postglacial Till
No. depth sediment thickness No. depth sediment thickness
thickness thickness

1208 | aA T 27.0

1997) a8 T 27.0 VES SNOENO)

ADO | BLA Toa 25.0

1299 15.5 LS 24.0 u -3 0 0
1200) a5o7 SA 25.0 ; : - e
NATL WAS oA on 26.0 ; a : ;
1302 b 5 Lea 0 0
1303. 14.9 T sz 6 10.6 0 0
1304089407 T : 7 11.6 0 0
OS. USL 1.0 z S all 209 0
1306 14.3 0.5 25.5 9 1207 5.5 0
IO WAL 1.0 24.0 10 8.9 0 0
OS WAS 1.0 25.5 11 9.5 5.5 0
1309 13.4 1.0 25.5

1310 14.0 0.5 25.5

Taakte Wels sa le SA 25.0

1312 15.2 2.0a 23.5

IGIGMN A AISNO 3.0a 22.5

1314 15.8 2.54, 22.5

INS SLA On 22.5

IS | G52 5.8 x:

1317 0815.2 6.0

1318 15.2 7.0 :

1319 15.0 Gus Z

1320 15.0 6.0 x

ey, a 6.0 se

1a70e 85.4 5.0 :

1323 9915.4 5.0 *

1324 9913.0 6.0 5

10S 1540 LAO 55

1326 15.0 3.0 5

1327 15.2 88 =

1328 15.0 os x

1329. 15.0 8.0 u

1930/0811550 6.8 53

1331.) 15.0 6.0 2

1332 14.5 5.0 :

1333 98 14,0 AS 8.5

1334 © 13.2 2.5 8.5

1S 19.0 10 8.0

1336 12.2 1.0 6.0

ge alae 0 3.0

1338 11.2 1.0 0

106

APPENDIX G

CALCULATIONS OF SEISMIC VELOCITY IN WATER

Core Measured Seismic Speed Core Measured Seismic Speed
No. depth Time No. depth Time
(m) (ms) (m/ms) (m) (ms) (m/ms)
50 16.0 21.177 1.511 71 16.0 20.962 1.526
51 14.0 18.676 1.499 72 13.6 17.386 1.564
53 13.4 19.118 1.401 75 15.8 20.909 Woevilal
54 15.2 19.706 1.542 76 10.7 13.750 1.556
55 18.0 22.647 1.589 77 15.6 20.682 1.508
56 15.9 20.295 1.566 78 15.4 20.228 1.522
58 10.4 13.382 1.554 80 10.5 13.296 Noo)
59 12.0 14.707 1.631 82 9.1 I SACS) 1.496
60 13.0 16.764 1.550 84 15.2 19.772 1.537
61 16.0 21.029 1.521 86 15.8 20.439 1.546
62 e710 22.500 1.564 87 15.3 19.863 1.540
64 15.1 19.176 1.574 89 13.4 17.472 1.533
67 20.7 26.591 1.556 92 13.9 17RD) 1.548
69 18.3 23.294 1.571 97 13.3 17.143 1.551
70 11.3 13.863 1.630 100 8.9 12.273 1.450

107

APPENDIX H

CALCULATIONS OF SEISMIC VELOCITY IN POSTGLACIAL SEDIMENTS

Core Postglacial Time to Seismic speed
No. sediment Pleistocene
thickness reflector
(m) (ms) (m/ms)
54 1.41 3.00 0.94
55 3.90 5.50 1.42
60 5.57 6.24 1.78
61 3.05 6.00 1.02
77 1.54 2.50 1.23
78 1.25 2.00 152)
79 0.80 i 5 eX0) 1.07
84 2.98 4.00 1.49
85 3.90 5.00 1.56
97 1.02 1.50 1.60
98 3.03 2.00 Wo dak
99 7 silts} 3.50 os)

108

APPENDIX I

COMPARISON OF POSTGLACIAL SEDIMENT THICKNESSES
AS MEASURED FROM THE CORES AND CALCULATED FROM THE SEISMIC RECORDS

Core Thickness
Net Seismic Measured Difference
(m) (m) (m)
51 2 5) 3.7 koZ
54 2.0 1.4 -0.6
55 3.5 308) 0.4
60 4.0 5.6 1.6
61 4.0 3.0 -1.0
73 0 0.3 08)
75 0 0.2 a2
76 1.0 0.6 -0.4
77 1.5 He) 0.0
78 apse) N53 -0.2
79 1.0 0.8 -0.2
81 3.5 3.0 -0.5
84 DoS) 3.0 0.5
85 68 358 0.3
86 2.0 od 0.1
92 Lo0) oul 0.1
95 4.0 4.0 0.0
96 3.0 D5) -0.5
97 1.0 1.0 0.0
99 2.5 Bod -0.3

109

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